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C I Borfh - Ca '^nn8 Stat* CmrSPE 

3; 56 Baietgii 




jasper L. Stuckey, State Geologist 

Bulletin Number 56 

Talc Deposits 


Murphy Marble Belt 




jasper L. Stuckey, North Carolina department of conservation and development 

H. S. rankin, Tennessee valley Authority 


North Carolina 

Department of Conservation and Development 

R. Bruce Etheridge, Director 

Division of Mineral Resources 

Jasper L. Stuckey, State Geologist 

North Carolina state Library 

Bulletin No. 56 * 


Earl C. Van Horn 

Prepared and Published in Cooperation with the Tennessee Valley Authority 

under the direction of 
Jasper L. Stuckey, North Carolina Department of Conservation and Development 

H. S. Rankin, Tennessee Valley Authority 




R. Gregg Cherry, Chairman Raleigh 

J. L. HORNE, Vice-Chairman Rocky Mount 

Charles S. Allen Durham 

J. Wilbur Bunn Raleigh 

Oscar P. Breece Fayetteville 

K. Clyde Council Wananish 

Geo. W. Gillette Wilmington 

W. J. Damtoft Canton 

Percy B. Ferebee Andrews 

A. H. Guion Charlotte 

W. Roy Hampton Plymouth 

R. W. Proctor Marion 

Miles J. Smith Salisbury 

D. M. Stafford Pomona 

A. K. Winget Albemarle 

Eric W. Rodgers Scotland Neck 

R. Bruce Etheridge, Director 



Raleigh, North Carolina 
November 22, 1948 

To His Excellency, Hon. R. Gregg Cherry, 
Governor of North Carolina. 


I have the honor to submit herewith manuscript for publi- 
cation as Bulletin 56, "Talc Deposits of the Murphy Marble 
Belt." This bulletin is another in the series being made possible 
by the cooperation of the Tennessee Valley Authority. 

The Murphy Marble Belt has produced varying amounts of 
high grade talc for more than 85 years. Although geological 
work has been done in the area at different times, this bulletin 
represents the first detailed geological report covering, as a unit, 
that part of the Murphy Marble Belt lying within the State of 
North Carolina. This report indicates that there are ample re- 
serves of talc in the area for long term operations, and it is be- 
lieved that the information contained herein will be of value to 
those interested in the area. 

Respectfully submitted, 

R. Bruce Etheridge, 






Purpose of Investigation 1 



Physiography T 2 

Transportation and Power 3 



Aerial Geologic Mapping 4 

Work Related to the Talc Deposits _' 4 

Ma j or Problems 5 


Phyllite and Mica Schist (pms) 6 

Quartz-ottrelite Gneiss (qog) 6 

Quartz-mica Gneiss (qmg) 7 

Mica Schist (ms) . 7 

Murphy Marble (mm) 8 

General Distribution 8 

Character of the Peachtree-Martin Creek Marble 8 

Extent and General Character of the Murphy Marble 9 

Zoning in the Murphy Marble 12 

Ottrelite Schist (os)„. 13 

Nottely Quartzite (nq) 14 

Ottrelite Gneiss (og) 14 

Staurolite-Mica Schist (stm) 15 

Quartz-Mica Schist (qms) 15 

Diorite (do) _' 15 

"Pseudodiorite" 18 



Original Deposition and General Structure 18 

Folds 19 

Faults 20 

Cleavages and Joints . 20 

Lineation 21 





Stratigraphic Control 22 

Structure 22 

Configuration of the Bodies .„ 22 

Controlling Structures 22 

Internal Structures 23 

Mineralogy of the Talc Deposits 23 

Talc 23 

Quartz 24 

Carbonate 24 

Amphibole 25 

Other Minerals 25 

Chemical Composition of the Talc 26 


Previous Interpretations 27 

New Diagnostic Criteria 28 

Genesis of Murphy Talc 29 



Location No. 1 30 

Location No. 2 30 

Location No. 3 32 

Location No. 4 32 

Location No. 5 32 

Location No. 6 32 

Location No. 7 34 

Location No. 8 37 

Location No. 9 : 37 

Location No. 10 37 

■ Location No. 11 44 

Location No. 12 44 

Location No. 13 44 

Location No. 14 44 

Location No. 1 5 44 

Location No. 16 44 

Locations No. 17 and No. 18 46 

Location No. 19 46 

Location No. 20 46 



Location No. 21 46 

Location No. 22 46 

Location No. 23 48 

Location No. 24 .* 48 

Location No. 25 48 

Location No. 26 48 

Location No. 27 48 

Location No. 28 48 

Location No. 29 49 

Location No. 30 49 

Location No. 31 49 

Location No. 32 49 

Location No. 33 49 

Location No. 34 49 

Location No. 35 49 

Location No. 36 ■. 50 

Locations No. 37 and No. 38 50 

Location No. 39 51 

Locations No. 40 and No. 41 51 


Locations for Prospecting 51 

Methods of Prospecting : 52 



Table 1. Chemical Analyses of Talc 27 

Table 2. Production and Cost Data — Carolina Talc Company 34 

Table 3. Talc Production — Nancy Jordan Mine 42 


Figure 1. Large quartz vein cutting quartz-ottrelite gneiss. Right 
bank of the Hiwassee River, opposite Lover's Leap, near 
Murphy. Looking northeast 7 

Figure 2. Overburden and solution cavities in quarry of the Colum- 
bia Marble Company, Marble, North Carolina 10 

Figure 3. Diorite (between the figure and the camera) , on the South- 
ern Railroad, pole No. 2331, 1.7 miles east of Hewitt. 
Looking south. 16 



Figure 4. 
Figure 5. 

Figure 6. 

Figure 7. 

Figure 8. 
Figure 9. 

Figure 10. 

Figure 11. 

Figure 12. 

Plate 1. 

Plate 2. 

Plate 3. 

Plate 4. 

Plate 5. 

Plate 6. 

Plate 7. 



Diorite, on right bank of Nottely River at Halls Ford, 
near Map Location No. 5. Looking southwest 17 

Sketches showing internal fractures in marble from Regal 
Quarry (after Loughlin, Berry, and Cushman). Arrows 
have been added to show relative movement and possible 
indications of overturning. Anticlines would be in direc- 
tion of hanging-wall sides 19 

Schematic cross-section showing relation of cleavages to 
folds in competent (C) and incompetent (I) rocks. Arrows 
indicate direction of relative movement along bedding 21 

Model showing underground workings at the Carolina Talc 
Mine. White parts of pegs represent talc encountered in 
drill holes. Looking northwest 33 

Mulberry Gap strip mine, looking southwest 35 

Flowsheet, Nancy Jordan Talc Plant, Hitchcock Corpo- 
ration 43 

Marble quarry of the Nantahala Talc and Limestone Com- 
pany at Hewitt. Looking northwest 


Diagrammatic section showing ideal location of explora- 
tory drill hole 52 

Diagrammatic plan detail of orientation of talc bodies and 
drilling control. Plan is taken at an elevation below top 
of rock. 53 


Plan of bedding at eleveation 1600, P. A. Mauney tract, 
Kinsey, North Carolina 31 

Underground workings, Minerals and Metals talc mine, 
Murphy, North Carolina 36 

Strip mine, Minerals and Metals talc mine, Murphy, North 
Carolina 38 

Plan of mine workings, Hitchcock Corporation, Nancy Jor- 
dan talc mine, Murphy, North Carolina 49 

Diagrammatic Sections, Hitchcock Corporation, Nancy 
Jordan talc mine, Murphy, North Carolina 41 

Core Hole layout, Section Six tract, Hitchcock Corporation 45 

Drill holes and mine shafts, Hartsfield property, Marble, 
North Carolina 47 


Geologic Map, talc deposits of the Murphy marble belt 

( 4 sheets ) Pocket 


Digitized by the Internet Archive 

in 2013 


By Earl C. Van Horn 


The Murphy marble belt extends some 35 miles in North Carolina from Wesser to the Georgia state 
line, including parts of Swain, Macon, and Cherokee Counties. Talc mining in the area is more than 
three-quarters of a century old and has persisted in spite of many difficulties. However, in recent years 
most of the mines and prospects have been abandoned and the utilization of talc resources has been at a 

The purpose of the current work was to find geologic criteria and establish methods for locating con- 
cealed talc and generally to sponsor and assist in the development of old and new talc resources and to 
acquire and apply new scientific and economic data. 

The Murphy marble formation, which is the only host formation to commercial talc in the area, is a true 
marble of nonuniform mineralogy, exposed as a part of the northwest limb of an overturned anticline. It 
is believed that the Murphy marble is conformable with adjacent rocks which comprise a series of schists, 
gneisses, and quartzites having distinct variations both along and across the strike and which are prob- 
ably of pre-Cambrian (?) Ocoee age. 

In addition to a revision of previous theories concerning the attitude of the Murphy marble, new data 
are presented concerning structural variations within the marble, and the marble formation has been sub- 
divided into lithologic units. Relationships between the marble and its contained talc deposits have been 
clarified to the extent of delimiting occurrences of commercial talc to a specific zone of the marble formation. 
It has been established that the attitudes of talc bodies are controlled by the attitudes of intraformational 
folds and are reflected in lineation phenomena. Theories are advanced to account for elliptical shapes of 
talc bodies. 

The mineralogy of the talc is discussed. It is proposed that the talc was formed by the actions of 
hydrothermal solutions rising from a granitic or dioritic magma, first silicifying a dolomitic rock and later 
effecting a replacement by talc without an intermediate chlorite or amphibole phase. It is further pro- 
posed that mineralizing solutions were given access by real or incipient weaknesses which were formed be- 
cause of an original dolomitic character of the central part of the marble. 

A geologic map of the marble belt and adjacent formations accompanies this report. A total of two 
operating mines and 39 prospects and abandoned mines are described in the text and marked on the geo- 
logic map. Results of diamond core drilling are described and correlated, and recommendations for fu- 
ture exploration work are presented. 


Talc deposits in western North Carolina occur in two settings. Deposits having the widest distribu- 
tion are associated with basic igneous rocks, particularly the olivine-bearing varieties in Macon and Jack- 
son Counties and pyroxene-bearing varieties in Madison County, but talc of this type has received little 
serious attention in the past. Of much greater importance are the deposits that occur as lenses and beds in 
very old dolomitic marbles in the counties of Swain, Macon, and Cherokee. This report is concerned only 
with the last named three counties. 


The North Carolina Department of Conservation and Development and the Regional Products Research 
Division of the Commerce Department of TVA established a cooperative program as a basis for this in- 
vestigation of the talc resources in the Murphy marble belt of the tri-county area. Specific purposes of the 
investigation were: (1) to develop criteria and methods for determining accurately the location of con- 

2 Talc Deposits of the Murphy Marble Belt 

cealed talc deposits; (2) to locate new talc reserves; (3) to assist property owners, investors, and operators 
in attaining higher efficiency in the exploration and development of deposits; and (4) to acquire and spon- 
sor the application of geologic and economic information that has not been available heretofore. 


All work was under the general direction of Mr. H. S. Rankin, Head, Minerals Research Section, Com- 
merce Department, TVA, and Dr. J. L. Stuckey, State Geologist, North Carolina Department of Conserva- 
tion and Development. Mr. E. L. Miller, Jr., of the North Carolina Department of Conservation and 
Development, was in the field during the summer of 1945, working principally in the vicinity of the Nan- 
tahala River and in the talc mines at Murphy, North Carolina. Mr. M. K. Banks, of TVA, assisted the 
writer from October 1945 to June 1946, and contributed especially to an understanding of the Nottely 
quartzite and the diorite sills. Dr. W. A. White, of the North Carolina Department of Conservation and 
Development, did petrographic work in the field during the summer of 1946. Any success resulting from 
this program would not have been possible without the splendid cooperation of all talc producers, owners, 
and mine personnel in the area. Special acknowledgment is due Messrs. J. W. Bailey, Jr., J. W. Bailey, Sr., 
F. C. Bourne, P. B. Ferebee, W. B. Hartsfield, and Jesse Ledford. The TVA Maps and Surveys Division 
prepared most of the plates and figures contained herein. Messrs. Benjamin Gildersleeve and B. C. 
Moneymaker, of the TVA, have kindly reviewed these writings, and the writer is grateful to Mr. C. E. 
Hunter, TVA, Dr. Jasper L. Stuckey, North Carolina State Geologist, and especially to Mr. Thomas L. Kessler, 
Geologist, Cartersville, Georgia, for their critical reading of the manuscript. The writer was in charge of 
this investigation from its inception in June 1945 to its completion in March 1947, and has performed 
most of the work. While the ideas contained herein are certainly not all his own, the writer assumes full 
responsibility for the information presented. Approximately half of the field work was spent in working 
with talc owners, operators, and investors. The remaining work was devoted to areal geology, mine map- 
ping, drill core studies, detailed study of talc occurrences, and related research. 


In North Carolina the Murphy marble belt extends some 35 miles from near Wesser, Swain County, 
southwestward across the northwest tip of Macon County, through Topton, Andrews, Marble, and Murphy 
in Cherokee County, to the state line. From the state line the marble has been observed southward in Geor- 
gia for nearly 50 miles to the vicinity of Canton, Georgia. Unless otherwise specified, subsequent discus- 
sion of the marble belt will refer only to that portion within North Carolina. 


The physiography of the area has not been worked out in detail, but in general it is characterized by 
inter-related low order straths. With few exceptions, stream valleys occupy, or are adjacent to, the marble 
belt. From the northeastern terminus near Wesser to the vicinity of Topton, the marble is exposed in the 
gorge of the Nantahala River, with numerous outcrops high on the northwest side of the gorge at elevations 
3,500 feet above sea level, or 600 feet above the river bed. From Topton southwestward to Murphy, the 
marble usually underlies the lowlands formed by the Valley River. From Murphy, the marble crosses a 
small divide between the Nottely and Hiwassee Rivers, underlies the Nottely River to near Ranger, and 
then is traced by small creeks throughout the remainder of its extent. Thus, general drainage patterns are 
controlled by the marble formation, but in detail the marble often is outside stream valleys, trending along 
adjacent slopes and across low divides. 

Keith 1 says the Nantahala River originally flowed down the Cheoah Valley along what is now Tulula 
Creek and was diverted by a branch of the Little Tennessee River working back along the Murphy marble. 
It appears equally possible that the Nantahala once flowed westward, through Red Marble Gap and down 
the present course of the Valley River. Large, well-rounded boulders of quartzite and vein quartz and 
smaller fragments of rocks typical of the upper reaches of the Nantahala River may be found along this 
course, which is coincident with the marble formation. 

1 Arthur Keith, U. S. Geol. Survey Atlas, Nantahala folio (no. 143), 1907, p. 1. 

Talc Deposits of the Murphy Marble Belt 3 

transportation and power 

Nearly all of the marble belt is situated satisfactorily with respect to transportation facilities. The 
Murphy branch of the Southern Railroad follows the belt from Wesser to Murphy, and U. S. Highway 19 
is seldom more than a few hundred yards from the marble over the same distance. To the west from Mur- 
phy, a branch of the Louisville and Nashville Railroad parallels the marble, as do several good state highways 
and county roads. Only between Ranger and Culberson is access to the marble formation at all difficult. 
Additional facilities are available as a result of the large number of conveniently spaced railroad sidings 
which are used for loading pulpwood along the two railroads. 

Electric power is readily available throughout the length of the marble belt. Between Culberson and 
Marble, TVA power is supplied by the cooperatives at Murphy and at Blue Ridge, Georgia. The Nantahala 
Power and Light Company provides electricity in all localities between Marble and Hewitt. 


Talc mining was begun in the Murphy marble belt in 1859 1 and has persisted in spite of many economic 
difficulties. There were no railroads in the area in those early days and the industry continued only so 
long as high prices justified the use of horse-and-wagon transportation. New sources of talc soon forced 
prices down to a level at which operations in North Carolina were no longer profitable, and mining was 
halted until the railroads entered the region in the late 1880's. 

As interest was revived, land owners and prospectors became familiar with those places where talc 
could be seen at the surface. Prospect pits and trenches were dug, abandoned, and reopened time and again. 
It appears that, from 1898 to 1928, only four or five talc "mines" were worthy of the name. These were: 
(1) the Hewitt Mine, near Hewitt Station on the Nantahala River, (2) the Valleytown Mineral Company 
mine, later the Biltmore Talc Company, two miles east of Tomotla, (3) the Hayes Mine at Tomotla, (4) the 
Hiliyer Mine, about one mile east of Kinsey, and (5) the Kinsey Mine at Kinsey (Map Location No. 5). In 
addition, almost the entire southeast slope of Talc Mountain at Hewitt was trenched and tunneled ("gopher- 
holed") for talc, with fairly successful results. The main production of talc was supplemented with small quan- 
tities of talc brought in by prospectors and sold in 100-pound lots to the larger producers. In 1927, the Notla 
Talc Company began an exploration program and developed the Carolina Talc Company mine just east of 
Kinsey. Production was begun in 1930, and, because of various peculiar conditions, the mine was closed 
in 1938 after a highly successful period of operation. 

In recent years most mines and prospects have been abandoned, and results of the search for larger 
and better talc deposits have been discouraging. The talc industry in western North Carolina did not 
nourish because of the following conditions : 

1. Many prospects have been located at sites having adverse surface and underground drainage and 
unfavorable bedrock conditions. Prospects have been opened on the banks and in the beds of streams 
because these are ideal places for talc to crop out and be seen easily. Many prospects and some mines 
(cf. Map Locations Nos. 17 and 18) were located in talc float which was from 10 to 100 feet from its source. 
It is not rare that much useless digging has been done because of the presence of a few talc scales (or, less 
rarely, sericite and chlorite scales) in the first few inches of top soil. 

2. Low, uncertain production has not been conducive to the use of suitable mining equipment. Prob- 
ably the chief cause of mine and prospect abandonment, where conditions otherwise were suitable, has been 
a lack of pumps, because many operations were begun "on a shoestring" and investment in adequate pump- 
ing equipment was rare. Similarly, hard rock has caused many prospects to be abandoned because of a 
lack of proper drilling equipment. Ordinarily, if simple pick and shovel work could not produce enough talc 
to pay its way, prospects never reached the proportions of mines. 

3. Owners and mine operators have not obtained suitable technological assistance, and their methods 
have been slow, costly, and relatively inffective. Plans of operation and theories of talc occurrence have 

1 J. H. Pratt, Talc and Pyrophyllite Deposits in North Carolina, North Carolina Geol. and Econ. Survev, Econ. Paper, no. 
1900, p. 8. 

4 Talc Deposits of the Murphy Marble Belt 

depended on legends and hunches, and core drilling has not been popular because of high unit cost and the 
failure to utilize information which could have been obtained from "dry" holes. Mine shafts have been 
poorly designed, and drifts and crosscuts were either too small in barren ground or too large where talc 
was encountered. 

It is apparent that the search for talc deposits heretofore has been fortuitous and unsystematic. Only 
since 1942 has there been a change in the general philosophy of exploring for concealed talc deposits. This 
is discussed further in the section on descriptions of the deposits. 



The geology of the area which includes the Murphy marble belt has been worked out previously only 
by Keith in the published Nantahala folio 1 , and in an unpublished folio on the Murphy quadrangle. In spite 
of the short time that Keith worked in this large area of complex, geology and rugged topography, his lith- 
ologic descriptions can be improved only through elaboration. 

In the immediate vicinity of the marble belt, Keith differentiated nine separate formations, designated 
as of Cambrian age, which he believed to occur in a major syncline. His oldest formation in the group 
was the Hiwassee slate, a dark, banded, micaceous slate having a thickness of more than 500 feet. He map- 
ped the Hiwassee slate only on the northwest side of his synclinical axis. The Great Smoky formation was 
shown as more than 6,000 feet of elastics which included conglomerate, sandstone, "graywacke", black 
slates, and quartz-, mica-, kyanite-, garnet-, and staurolite schists and gneisses. The Nantahala slate was 
mapped as nearly 2,000 feet of black slates and kyanite-, staurolite-, and garnet schists. The Tusquitee 
quartzite was described as from 20 to 500 feet of dense white quartzite. The Brasstown formation consisted 
of about 1,000 feet of dark gray or black ottrelite schist and slate, and lighter-colored mica schist. The Val- 
leytown formation was mapped as 1,000 feet of garnet schist, "graywacke", ottrelite schist, and slate. The 
Murphy marble was shown as pure limestone and dolomite ranging in thickness from 150 to 500 feet. 
Immediately on either side of the synclinal axis Keith mapped the Andrews schist, comprising 200 to 500 
feet of calcareous ottrelite schist and limonite beds. The central part of Keith's syncline, and youngest forma- 
tion of the series, was the Nottely quartzite, mapped as about 150 feet of white quartzite. Excepting the 
Hiwassee slate and the Murphy marble, all formations were shown as being repeated on each side of the 
synclinal axis. The missing limb of the Murphy marble was explained by a major thrust fault which has 
since been known as the Murphy Fault. The occurrences of marble southeast of the Murphy Fault were 
mapped as fault outliers. 

To the southeast of the series described above, Keith mapped the Archean Carolina gneiss, a complex of 
schists, gneisses, and granitoid layers, characterized in that area by intricate crumpling and folding. 


Pratt 2 made a general study of the talc deposits of the belt in 1899. His opportunities for seeing the 
talc in place were rather limited, and his conclusions apparently were influenced by the testimony of mine 
workers and by the examination of unsatisfactory exposures ; for instance, he confused the Nottely quartzite 
with siliceous phases of the Murphy marble. Several years later, Arthur Keith studied talc occurrences 3 in 
connection with his geologic mapping in the southern Appalachians. He interpreted the geology of the talc 
in greater detail than did Pratt, but did not have sufficient time in the field to obtain a clear picture of the 
many problems involved. 

Studies of associated brown iron ores by Bayley 4 , and of associated limestones by Loughlin, Berry, and 
Cushman"' have contributed indirectly to a knowledge of the talc deposits, chiefly through observations of 

Arthur Keith, 1907. 

J. H. Pratt, 1900. 

Arthur Keith, Talc Deposits of North Carolina, U. S. Geol. Survey Bull. 213, 1903. 

, U. S. Geol. Survey Atlas, Nantahala folio (no. 143), 1907. 

W. S. Bayley, Deposits of Brown Iron Ores in Western North Carolina, North Carolina Geol. and Econ. Survey, Bull. 31, 19 25. 
G. F. Loughlin, E. W. Berrv, and J. H. Cushman, Limestones and Marls of North Carolina, North Carolina Geol. and Econ. 
Survey, Bull. 28, 1921. 

Talc Deposits of the Murphy Marble Belt 5 

lithology and mineralogy in adjacent formations. More direct and important knowledge of the talc was sup- 
plied by Stuckey, who, in following up his work on pyrophyllite in North Carolina, made petrographic studies 
of the Murphy talc but did not include detailed surveys of the various deposits 1 . Gillson 2 and Moneymaker 1 
contributed ideas on the origin of the Murphy talc on the basis of published reports of field work by Pratt, 
Keith, and Stuckey. 


Results of the present work indicate that Keith's interpretation of structural and age relations of the 
rocks of the Murphy marble belt are erroneous, at least in part. To increase the complexity of the problems 
involved in this investigation, work subsequent to Keith's has been based on his geologic time scale, and 
errors, therefore, have been accumulative. Although the work which is reported in the present discussion 
has been restricted to a small part of the area involved and is not of a nature to solve the many general 
problems, it is believed that the results obtained will contribute to a more accurate understanding of the 
areal geology. 

In their work on the geology of the Appalachian region, G. W. and Anna J. Stose have taken a broader 
view of the problems at hand. Expanding on their own work, and on the work of Safford, Hayes, and Crick- 
may 4 , as well as of Keith"', the Stoses have established a currently accepted theory that the series from the 
Hiwassee slates through the Valley town formation are of pre-Cambrian (?) age and may be identified as 
Ocoee series. They conceded the possibility that Keith's Nottely quartzite, Andrews schist, and Murphy 
marble might be of Lower Cambrian age, but suggested that the Nottely quartzite is the oldest and the Murphy 
marble the youngest of the three formations, and that the iron-bearing Andrews schist may be transitional 
between the quartzite and the marble. Also, they suggested that this trio may represent a window exposed 
in the Great Smoky overthrust block (Ocoee age)' 1 . 

In general, the age relationship of the rocks of the area would be of little consequence insofar as the 
economics of the talc deposits are concerned, but, as will be seen later in discussions of lithologic phases 
and of the location of talc deposits within the marble formation, a basic concept is in need of clarification 
since the three dimensional position of the marble, and consequently of the talc deposits, is involved. It is 
important to solve the question of the presence or absence of one or more major stratigraphic faults, as well 
as the type of major folding, whether synclinical or anticlinal, since these problems have a direct bearing on 
the occurrence and position of concealed talc bodies. The resolution and/or revision of all these theories will 
guide future geologic work in the area and assist in developing more accurate methods of prospecting for 
mineral resources. 


A full understanding of the marble formation and its contained talc requires a rather precise picture of 
the formations immediately adjacent to the marble, and a somewhat broader view of the over-all series of 
rocks of the area. Areal geologic mapping was carried out accordingly, with detailed work in the central 
portion of the belt, and more general studies in the outer areas. In the more rugged country, the scope of 
this program did not permit thorough survey work, and Keith's mapping was depended upon to some 

J. L. Stuckey, Pyrophyllite Deposits of North Carolina, North Carolina Dept. Cons, and Dev. Bull. 37, 192S. 

, Talc Deposits of North Carolina, Econ. Geology, vol. 32, no. 8, pp. 1009-1018, 1937. 

J. L. Gillson, Origin of the Vermont Talc Deposits, Econ. Geology, vol. 22, pp. 246-287, 1927. 
, Talc, Soapstone, and Pyrophyllite, AIME, Industrial Minerals and Rocks, pp. S73-S92, 193S. 

B. C. Moneymaker, Talc Deposits of North Carolina (discussion), Econ. Geology, vol. 33, no. 4, 193S. 
J. M. Safford, Geology of Tennessee, 1869. 

C. W. Hayes, Overthrust Faults of the Appalachians, Bull. Geol. Soc. Am., vol. 2, pp. 147-149. 

G. W. Crickmay, Status of the Talladega Series in Southern Appalachian Stratigraphy, Bull. Geol. Soc. Am., vol. 47. pp. 13 71- 

Arthur Keith, The Great Smoky Overthrust, Bull. Geol. Soc. Am., vol. 3S, pp. 154--155. 

G. W. and Anna J. Stose, The Chilhowee Group and Ocoee Series of the Southern Appalachians. Am. Jour. Sci., vol. 242. pp. 
367-390 and 401-416, 1944. 

6 Talc Deposits of the Murphy Marble Belt 

In the present work, overlapping and subdivision of previously mapped units will be apparent. It 
should be kept well in mind that gradation, rather than abrupt change, is common among the rock types in 
the area described, and unit boundaries are not everywhere distinct in the field. The nature of the rocks 
of the area bears out older conceptions of comparatively rapid erosion and ebb-and-flow deposition of the 
original sediments, with intervening periods of quiescense. It follows that difficulty must be expected in 
correlating small lithologic units from one locality to another, and that the various facies should be con- 


sidered only as lithologic tendencies of rocks that originally were laid down under constantly changing con- 
ditions of sedimentation, and which subsequently were affected by equally non-uniform conditions of meta- 
morphism. Consequently, the term "formation" is used with reservation in discussions which follow. 


Located northwest of the marble belt, as shown on the accompanying geologic map, is a series of rocks 
which formerly was included in Keith's Nantahala slate. Typically, the rocks are dark, banded phyllites 
("slates") containing pyrite, staurolite, ottrelite, graphite, hornblende, biotite, and occasional garnets. The 
northwestern (upper) portion of the formation tends toward a fine-grained, sericitic schist which has repe- 
titive zones of the other rock types. Usually confined to the more phyllitic portions are thin beds of dark, 
massive, micaceous quartzite, called "graywacke" by Keith. This quartzite commonly is medium-grained 
and arkosic and conglomeratic in places. On the southeast side (base) of the formation there is from 50 to 
300 feet of massive quartzite-conglomerate. Also contained in the phyllites are gabbroid dikes or sills up 
to four feet thick and at least 20 feet along the dip. Their extent along the strike could not be observed. 
The rock is dark, coarse, predominantly hornblende and augite with smaller quantities of chlorite and ver- 
miculite, and it appears to have been hydrothermally silicified. Many of the occurrences are adjacent to 
minor fold axes. 

The character of the formation changes northeast from the town of Marble and southwest from the 
town of Murphy, reflecting original non-uniform lithology, and probably reflecting late alteration by hot 
solutions of deep-seated origin. Northeastward, to about the vicinity of Topton, the phyllites become more 
schistose and lose much of their accessory mineral content. From Topton to Wesser the formation gains 
quickly in both silica and carbonate, and gradation into the quartz-ottrelite gneiss, described below, is prob- 
able. Variations southwest of Murphy are less noticeable except for a darker color and an increase in 
silica content. 

As in most of the other rocks of the area, internal structures are dominated by a major foliation dip- 
ping 45° to 90° southeast, along which considerable movement has taken place. Although small bedding 
faults and shear zones may be observed, it is likely that much of the stress to which the rocks have been 
subjected has been relieved along foliation planes. Several zones of minor folding have been noted but no 
major intraformational folds have been recognized. 


This formation crops out in the central part of the area under consideration. It is a part of Keith's 
Brasstown formation and appears as a dark, quartz-ottrelite-garnet gneiss containing biotite, hornblende, 
magnetite, and nodules and stringers of "pseudodiorite". Much of the quartz may be secondary, and a high 
sericite content in some parts of the rock may be the result of hydrothermal action. At several places the 
rocks are cut by quartz veins, up to six feet thick, which are accompanied by no accessory minerals other 
than thin scales of ilmenite and small patches of fine muscovite (Fig. 1). The quartz appears to lie in 
high-angle strike joints, though occasional blebs invade minor strike shear zones. The gneiss formation is 
more uniform across the strike than is the phyllite and mica schist described above, but changes along the 
strike are more pronounced. Schistosity increases markedly and the ottrelite content diminishes southwest- 
ward from Murphy. In the vicinity of the Nantahala River, the rocks appear to grade into the formation 
above, and the calcite content becomes high. 

1 Parenthetical script refers to symbols appearing on the accompanying geologic maps. 

Talc Deposits of the Murphy Marble Belt 


Fig. 1. — Large Quartz Vein Cutting Quartz-Ottrelite Gneiss. Right 

Bank of the Hiwassee River, Opposite Lover's Leap, 

Near Murphy. Looking Northeast. 

Besides the major foliation already mentioned, flow cleavage and a lineation of cleavage intersections 
are prominent in the less massive beds. Large joint systems are rare and much of the imposed stress 
seems to have been absorbed along foliation planes. 


These rocks are more persistent as to type than any of those discussed above, probably because of their 
dense nature. Even the more schistose zones show quartzitic and conglomeratic relics. Although essentially 
gneiss, the formation contains massive quartzite which has been utilized, in more accessible locations, for 
rock quarries in state highway work. "Pseudodiorite", hornblende, and biotite are rather abundant in 
these quartzitic zones. Sericite is common in all of the formation, and ottrelite occurrences are not rare. 
The ottrelitic zones commonly contain garnet. Near the southeast contact of the gneiss, there is found an 
unusual type of arkosic quartzite that contains fragments of plagioclase. Most of the plagioclase seems 
detrital, but some of it has the appearance of secondary growth or rejuvenation as in the Hiwassee slate 
east of Irwin, Tennessee, and in the Little River slate near Lincolnton, Georgia 1 . Under the microscope it 
was noted that occasional metacrysts of secondary muscovite and chlorite are present. Whether by cause 
or by chance of observation, this secondary mineralization was especially noticeable in the vicinity of diorite 
outcrops and known talc occurrences. 

Because of its dense, competent nature, the formation does not have well developed foliation planes as 
do the surrounding rocks, but an orientation of mineral grains is present. Small thrust planes and shear 
zones are common, as are systems of dip and oblique joints. Probably the most characteristic structure 
of the formation is a persistent zone of flat-lying, recumbent folds which suggest plastic deformation, some 
of the folds being unbroken and tightly closed for a distance of more than 20 feet along the dip. 2 


Separating the quartz-mica gneiss from the Murphy marble is 200 feet or more of fine-grained, uni- 
form mica schist which seems to represent a large shear zone. Probably related to the secondary mineral- 
ization just described are more or less random injections of pegmatite material, composed principally of 

1 C. E. Hunter, Personal Communication. 1947. 

- Similar structures have been observed by the writer in many parts of the Great Smoky formation of North Carolina and in the 
Pigeon slate of Polk County, Tennessee. 

8 Talc Deposits of the Murphy Marble Belt 

plagioclase and quarts, but also including muscovite crystals up to one-half inch across. The material is 
distributed in migmatitic fashion through the rock. 

Like the quartz-mica gneiss, with which it is included in Keith's Valleytown formation, the mica schist 
changes little along the strike. Thin quartzitic laminae become progressively numerous from Ranger to 
Culberson and the mica is somewhat coarser. In the interval between Hewitt and Wesser, the schist con- 
tains thin calcareous beds which give way to slate and quartzite to the northeast. * 

The formation is characterized by a prominent foliation, each plane of which has slickenside striae 
and a lineation of cleavage intersections, although lineation is difficult to recognize east of Hewitt. The pres- 
ence of large diorite sills (See Page 14), just east of Hewitt and at Halls Ford at Kinsey (Near Talc Local- 
ity No. 5), indicates that contact with adjacent quartz-mica gneiss may be a major fault. 


As the Murphy marble is the only formation that contains talc deposits in the area, it is the formation 
with which this bulletin is most concerned and it will be described, therefore, in greater detail than are the 
other formations. Keith's terminology 1 is followed here because the formation is widely known and there 
is little chance of confusion with other rocks. The current work has resulted in a revision of structural 
interpretations, and has added to previous conceptions of the location, lithology, and mineralization of the 

General Distribution — In North Carolina the Murphy marble occurs in two geographically separated 
areas. The first and main belt extends from near Wesser to Culberson and on into Georgia, following along 
the Nantahala, Valley, and Nottely Rivers. The outcrop pattern is locally irregular as the result of domed 
and plunging folds and varying degrees of topographic re-entrant, and the marble is found both in stream 
bottoms and on the slopes. A second marble area is reported to extend from Peachtree, down Calhoun 
Branch and across Hiwassee River, thence following a narrow belt along Little Brasstown Creek to Martins 
Creek School 1 , thence curving north down Martin Creek and west up West Fork of Martin Creek, thence 
down the headwaters of Caney Creek and possibly curving across to and down Gold Branch to Nottely 
River 2 . This stretch of marble, which will be described first, is a possible extension of the Cutcane Creek 
belt just to the southwest in Georgia 3 , but evidence of a direct connection is lacking southwest of the Nottely 
River at Gold Branch. 

Character of the Peachtree-Martin Creek Marble — Outcrops of these rocks are rare and previous map- 
ping seems to have been based on indirect indications almost throughout. The few available exposures 
show light to dark gray banded marble, sometimes fairly pure but more often micaceous, and gray calcare- 
ous schist. Siliceous phases have not been observed. The rocks usually are fractured, with healing by calcite, 
and there is evidence of small and large folds which probably account for the sinuous trend of the forma- 
tion. Adjacent rocks are pyritic ottrelite gneiss and ottrelite schist that contain limonite beds in the 
residuum, and finer grained mica schist, quartz-mica schist, and mica slates. Hypogene alteration is indi- 
cated in the rocks of the area by secondary quartz and sericite, and by epidote in associated siliceous boul- 
ders. On the property of A. Q. Ketner, near a cemetery just north of Martin Creek School, samples re- 
ported to be talc were taken from a field about 300 yards south of a marble exposure. The samples came 
from bed rock which is a relatively pure sericite schist well removed from a marble formation. The rock 
has many of the properties of talc and may contain a very small quantity of talc mineral, but sericite con- 
stitutes the mass. Bayley was told 4 that talc had been found at the mouth and near the headwaters of Gold 
Branch, but the writer could not find similar evidence either in the field or from persons living nearby. 

Because of concealment afforded by recent stream deposits, upper terrace gravels (west of Macedonia 
Church), and generally deep overburden, it was decided early in the program that further work would be 
confined to the first and main marble belt which passes through Murphy, and work in the Peachtree-Martin 
Creek area was discontinued until the time when new road cuts, water wells, scoured stream beds, and 

I Arthur Keith, 1907. 

- W. S. Bayley, op. cit., 1925, p. 62. 

II Laurence LaForge and W. C. Phalen, op. cit. 
1 W. S. Bayley, 1925, pp. 61-62. 

Talc Deposits of the Murphy Marble Belt 9 

other features will afford additional information. Future references to the Murphy marble belt in this 
report will exclude the Peachtree-Martin Creek area unless otherwise specified. 

Extent and General Character of the Murphy Marble — Previous workers usually have referred to the 
Murphy marble as a formation consisting entirely of pure, rather fine-grained, recrystallized marble, more 
or less dolomitic, grading into mica schist on one side and ottrelite schist on the other, not uniform in color 
but predominantly white, and in places faulted out entirely (northeast of Andrews). "Its freedom from 
argillaceous and sandy materials, such as make up the entire bulk of the preceding formations, shows that 
the geographic conditions changed abruptly and entirely at that time." 1 

It has now been found that the Murphy marble is neither homogeneous nor unsymtematically hetero- 
geneous, but that it is probably zoned in accord with accepted principles of sedimentation and petrology. It 
has been found also that facies which were originally sandy and shaly are important features of the forma- 
tion and sometimes nearly displace the calcareous facies. A formation may be absent from its normal posi- 
tion in a sequence for one of three reasons: (a) the material was never deposited, (b) the material was 
deposited and later eroded, or (c) the material was deposited and later faulted out of position. Of course, 
the formation could be present and merely concealed from view. Faulting has been used in the past, with 
supporting evidence, to explain the apparent absence of the Murphy marble in certain localities, but equally 
good evidence now supports reason (a) in some places, and the problem of concealment cannot be ignored 
in others. 

At the North Carolina-Georgia state line the marble is less than 200 feet thick. There are no good ex- 
posures, but indications are that much of the formation is represented by quartzite and mica schist, as it 
is a mile to the southwest in Georgia. Crossing the northern edge of Culberson, the marble follows a series 
of low depressions and is exposed in a quarry and railroad cut just west of where the Louisville and Nash- 
ville Railroad crosses Rapiers Mill Creek. It follows down the Nottely River past Ranger to a big bend 
in Nottely River at Stockade Mountain, and appears only as soft, white, calcareous material in stream 
beds and as calcareous schist at its transition into adjoining rocks. In the railroad cut in a low gap in a 
bend of Nottely River at Stockade Mountain there are several large, fresh outcrops of light-gray, tremolitic 
marble containing thin partings and scales of white talc and small blebs of vein quartz. Fragments of talc 
occur in the overburden but these seem to have been transported, at least in part, from higher up the slopes 
of the mountain. These outcrops are less than 50 feet from the marble-mica schist contact. About 1,000 
feet west of Kinsey Station, in the same river bend, a small ledge of white and light-gray, fine-grained mar- 
ble is in the bank of an abandoned quarry on the southwest side of the railroad. 

The largest marble exposure in this section is in the Kinsey quarry (Map Location No. 5) though the 
marble can be seen only as irregular blocks on the south side. These include gray, blue, pink, and white 
varieties that are fine- to coarse-grained, both pure and with schist laminae up to three-fourths inch thick. 
Accessory muscovite, tremolite, actinolite, phlogopite, biotite, and pyrite are present. The most southeast- 
erly exposures contain lentils or beds of talc up to 12 inches thick. A ledge of silicified marble measures 
four feet thick. The Kinsey talc mine is located at this quarry and will be described later. 

At the Carolina talc mine, 3,000 feet to the northeast, white, fine-grained marble and dark, serpentin- 
ized (?) slates can be found on the mine dumps, but there are no surf ace exposures. Across Mulberry Gap, 
in a second bend of Nottely River, about 40 feet of weathered sandstone crops out at the Mulberry Gap 
mines of Minerals and Metals Corporation. This rock probably represents marble that has been completely 

From Mulberry Gap, the marble generally follows down the Notteley River in which are occasional 
white marble ledges rising above the sandy bottom. Transitional calcareous beds are found in ledges of 
ottrelite schist along the old Louisville and Nashville Railroad bed. A small ledge of decomposed impure 
marble appears in the bed of Caney Creek, but from the valley of the Nottely River the marble can be traced 
northeastward only by talc exposures and topographic expression until it reappears in the bed of the Hi- 
wassee River. In this interval it trends through Nancy Jordan Gap and the Hitchcock Corporation's Nancy 
Jordan and Cold Springs talc mines. At Section Six (Prospect No. 13 on Geologic Map) only transported 
talc appears on the surface, but a few small ledges of silicified marble can be seen in the bed of nearby Brit- 

1 Arthur Keith, 1907, p. 6. 


Talc Deposits of the Murphy Marble Belt 

tain Branch. Here also are dumps from old marble pits where lime was burned many years ago. Gold- and 
galena-bearing quartz veins have been reported at this location 1 , and recent diamond drilling disclosed 
small galena-filled joints in white, fine-grained marble. A churn-drilled water well at Prospect No. 14 con- 
firmed the location of the formation by intercepting dark blue, graphitic marble underlain by gray, med- 
ium-grained marble. At Prospect No. 15, a ledge of silicified marble crops out in the railroad cut beside 
J. B. Moore's house, and it is reported that white marble was intercepted by a, diamond drill about 1,000 
feet further northeast. 

Gray, banded marble is exposed along a small stream, immediately west of Regal Station, by pits 
which were made in search of dimension marble. The famous Regal marble quarry, 400 feet southeast of 
Regal Station, is now filled with water, but it has been described in bulletins of the North Carolina Geolog- 
ical Survey 2 . This is the source of the Regal blue marble of which the Murphy courthouse is constructed. 
Blue and gray marble is reported to have contained graphite, amphibole, pyrite, quartz, and talc in small 
grains. Waste blocks, piled around the quarry, show many of these accessory minerals and also the 
cleavage, joints, and drag folds described by Loughlin, Berry, and Cushman 3 (See Fig. 5). The Regal 
quarry is situated near the stratigraphic base of the overturned formation (See Discussion of Folds, Page 
40), and southeast of where the talc-bearing zone normally would be exposed. 

Between Regal and Marble the formation can be traced by means of talc prospects and the positions of 
adjacent formations. One exposure of light-colored, tremolite-bearing marble is found on the Hayes prop- 

Fig. 2 — Overburden and Solution Cavities in Quarry of the Columbia 
Marble Company, Marble, N. C. (Photo by E. L. Miller, Jr.) 

erty at a gauging station on Valley River at Tomotla. Near the mouth of Sam Branch, in a northeast-plung- 
ing anticlinal structure, a churn drill struck white marble at a depth of 26 feet. A southwest-plunging 
anticline is revealed in a marble quarry on Bettis Branch in the village of Marble. This dimension grade 
marble is light gray, of medium to coarse grain, and has small amounts of tremolite and pyrite. The grada- 
tional contact between marble and mica schist is quite clear in the crushed stone quarry farther to the 
north where siliceous and micaceous marble contains much muscovite and biotite and a few small grains 
of feldspar. 

A small ledge of mottled white, fine-grained, dolomitic marble occurs in Hyatt Creek, 100 feet north 
of the highway. Beyond this point, the width of the area underlain by the marble increases greatly owing 
to a series of northeast-plunging folds, and the formation probably increases in true thickness as well. It 
is in this area that quarries of the Columbia Marble Company were located in the desirable blue marble. 
All but a recently opened quarry have been abandoned because of heavy water flow and excessive jointing, 
but information can be obtained from a study of the waste material. Only a rather coarse-grained rock is 
suifable for quarrying so that representative samples of the entire formation are lacking. The predomi- 

1 J. L. Stuckey, 1937, n. 1067. 

2 T. L. Watson and F. B. Laney, The Building and Ornamental Stones of North Carolina, N. C. Geol. Surv. Bull. no. 2, 190 6. 

G. F. Loughlin, E. W. Berry and J. A. Cushman, op. cit. 
8 Idem., pp. 38-40. 

Talc Deposits of the Murphy Marble Belt 11 

nating colors are blue and gray, and the stone, which contains individual calcite crystals up to three-eighths 
.of an inch across, probably has a low magnesia content. Tremolite, and large cubes and small grains of 
pyrite are the usual accessories, occurring without regular orientation. Occasional blocks of finer-grained 
marble contain secondary mica and phlogopite and occasional splotches of secondary calcite. These rocks 
are mostly white, but in places are mottled with a pink color which may result from manganese impurities. 

In the summer of 1946, the writer examined the last of the old Columbia quarries, immediately north 
of the machine shop, just before it was abandoned. Overburden from five to ten feet thick barely covered 
rock pinnacles which had an average relief of about five feet (Fig. 2). Enlargement of joints by solution 
seldom exceeded six inches and the largest cavities were approximately ten feet long by two feet wide. 
Most of the fractures were of an irregular incipient nature. The marble was of medium blue-gray and 
light-gray color, coarse-grained, with a faint banding which indicated the crest of an anticline plunging 
four degrees northeast. The newest quarry, now being opened, is barely inside the northwest edge of the 
Murphy marble on Welch Mill Creek, where bedrock occurs under ten feet of stream gravel and boulders. 
Medium-grained marble of white to light gray color contains random pink zones one to four feet thick. The 
attitudes of different beds reflect a series of northeast-plunging folds. Natural ledges of similar rock may 
be seen just across the creek to the east. 

At the home of C. H. Townson, on a knoll south of the highway and a little west of north from the 
mouth of Welch Mill Creek, a dug well is reported to have bottomed in white marble at 50 feet, but a drilled 
well 40 feet away passed through white, tremolitic marble at 78 feet, and remained in feldspathhic ottrelite 
schist to a depth of at least 140 feet. At the first house east of Coalville Crossing, a drilled well showed 
white marble from 11 feet to at least 60 feet below the surface. 

Both southwest-plunging folds and northeast-plunging folds are present in the area between Coalville 
and the western edge of Andrews ; to the east from Andrews nearly all folds plunge to the northeast. Gray 
banded marble is exposed on a dirt road northeast from Valleytown Cemetery across Junaluska and Worm 
Creeks, and a few slabs of fine-grained white marble can be seen in Junaluska Creek southwest of Valley- 
town. Nearly all mapping of the marble between Coalville and Rhodo has been based on outcrops and 
structures of adjoining rocks. 

Gray, medium-grained marble is exposed in a small abandoned quarry on the south side of Totherrow 
Branch at Rhodo. On the highway just west of the mouth of Jenkins Creek, thin marble beds have been 
seen in a strongly sheared, quartz-injected, black slate. From the mouth of Jenkins Creek to Nelson Creek 
fine-grained, white and gray, badly fractured marble occurs in ledges and in talc prospect pits. Much of 
this marble shows encroachment of originally sandy and shaly facies, until at Red Marble Gap the entire 
Murphy marble formation is represented by a white, leached, quartzite and mica schist totalling 25 feet 
thick. Equivalent thinning is reflected in the Nottely quartzite and the intervening mica schist. 

From Red Marble Gap to a point opposite Rowlin School, the formation is obscured, but apparently it 
gradually thickens as the carbonate facies is resumed. Continuing on to Handpole Branch, marble is ex- 
posed regularly in several different belts as the result of repetition by northeast plunging folds, with cal- 
careous, siliceous, and micaceous facies present. Notable are a large exposure of pink marble in a draw 
north of the railroad 1,300 feet west-southwest of the junction of U. S. Highway 19 and the Nantahala 
Powerhouse road and a white, siliceous, talc-bearing marble containing bluish quartz grains on the high- 
way 300 feet west of the Swain-Macon county line (Talc Prospect No. 31). 

Between Handpole Branch and Blowing Spring the marble formation attains a thickness up to 350 
feet as it trends well up on the slopes above Nantahala River, exhibiting an irregular outcrop pattern from 
topographic re-entrants and constantly changing dips and strikes. Siliceous and micaceous facies occur 
erratically, and differences in the degree of alteration are reflected in zones of high muscovite, chlorite, 
amphibole, or talc content, as mentioned in later descriptions of talc prospects. 

As is forecast by the apparent termination of the Nottely quartzite, the marble thins sharply to the 
east of Blowing Spring and disappears entirely beyond the peak shown as Bushnell No. 8. Wide expanses 
of adjacent rocks are quite calcareous farther on but it is not likely that they represent the Murphy marble 
as a formation. Rather they seem to reflect either the beginning or ending of the region's carbonate source. 

12 Talc Deposits of the Murphy Marble Belt 

Zoning in the Murphy Marble — Natural outcrops of the Murphy marble are so widely separated that the 
preparation of detailed geologic sections across the entire formation has been comparatively futile in the 
past. However, a careful study of the results of recent core drilling programs, coupled with the combined 
results of old and new geologic field work, has shed new light on the stratigraphy of the marble. Detailed 
core logs are now available from 12 holes in the vicinity of Hewitt, 6 holes at Marble, 5 holes at Section Six, 
east of Murphy, 20 holes at Hitchcock Corporation's Nancy Jordan talc mine, west of Murphy, 16 holes 
at the mine of Minerals and Metals Corporation on Nottely River, and 16 holes on the P. A. Mauney prop- 
erty west of Kinsey. The average depths of holes range from around 75 feet at the Minerals and Metals 
mine to well over 200 feet at Hitchcock Corporation's property. The most useful of the drilling programs, 
as a source of stratigraphic information, was on the P. A. Mauney property where 250 feet of an estimated 
total of 350 feet of marble section was cored. 

Diamond drilling at the Hitchcock Corporation property (Location No. 10) gave the first indication of 
a stratigraphic sequence within the marble. When the first several holes were found to be amenable to 
correlation, the new-found data were applied successfully in outlining part of a large talc body, and unex- 
pected additional reserves were forecast and later proven. The average section, converted to true thick- 
ness (perpendicular to the bedding), from top to bottom of the local attitude, was as follows: 

40 Feet of blue-black to bluish-gray, coarse-grained, graphitic marble, occasionally stylolitic, 
with short (2mm) tremolite needles and rarely grains or clusters of pyrite. (Blue zone). 

20 Feet of medium to light gray, medium-grained marble, sometimes stylolitic at top, with trem- 
olite needles up to 10 mm long. (Gray zone). 

15 Feet of light bluish-gray, fine-grained, lustreless marble, with or without tremolite, which is 
given a distinctive mottled appearance because of a myriad of small internal fractures. (Mot- 
tled zone) . 

45 Feet of white, medium to fine-grained dolomitic marble. This is the zone which is often 
partly silicified and which contains commercial talc deposits. (Talc or white zone). 

25 (plus) Feet of mixed, sometimes banded, gray and white, medium to coarse-grained marble 
which contains thin beds of pink marble and accessory pyrite, phlogopite, actinolite, quartz, 
tremolite, muscovite, chlorite, and scapolite. (Mixed zone). 

While drilling was in progress on Hitchcock Corporation property, a diamond drill program was begun 
by the Mauney Mining Company on property of P. A. Mauney (Location No. 4) and 12 holes were drilled 
at random in the northwest half of the marble belt. After an analysis of the Hitchcock drilling was ex- 
plained, the Mauney Company drilled four additional holes in the desired location and disclosed a section 
which was practically identical to that on Hitchcock property. 

Beginning at the bottom of the section just listed, the first stage of the Mauney Company's drilling 
showed marble zones as follows: 

25 Feet of light and dark gray, banded, argillaceous marble, often jointed and brecciated, with 
accessory biotite, chlorite, and muscovite, and small specks of talc. (Slaty zone). 

85 Feet of medium- to fine-grained marble, having intermittent zones of white, pink, and gray 
color, nearly all of which is characterized by the presence of actinolite clusters and pyrite, and 
which has considerable phlogopite in the lower portions. Sand grains, secondary quartz, and 
small scales of talc occur at random. (Actinolite zone). 

20 Feet of dark micaceous marble and thin slate and schist laminae, having pyrite, chlorite, 
biotite, and muscovite. (Transition zone). 

That portion of the marble section above the blue zone has not been cored, and correlation has been 
based on exposures principally in the bed of Hiwassee River at Murphy and in the quarries at Marble. From 
the ottrelite schist to the blue marble zone it is estimated to be as follows : 

25 Feet of fine- to medium-grained white and light-gray marble, containing ottrelite and phlog- 
opite, and having interbedded calcareous schist in the upper portion. (Transition zone). 

25 Feet of white, medium- to coarse-grained marble having tremolite and pyrite. (Coarse white 

30 Feet of gray, coarse- to medium-grained marble having tremolite and pyrite. (Coarse gray 

Talc Deposits of the Murphy Marble Belt 13 

After the Murphy marble had been subdivided, drill hole locations were laid out on the J. W. Bailey 
property, 500 feet south of the Mulberry Gap Mine (Location No. 7), and at the Section Six property (Lo- 
cation No. 13), with the result that core records conclusively substantiated previous findings. Similar cor- 
roboration was experienced on the Hartsfield property (Location No. 25) near Marble, except that the 
sequence was reversed since the beds were in their normal position instead of being overturned (See Page 
19), and only parts of the white, mottled, and gray zones were cored. Core drilling at Hewitts was less 
successful only because excessive core loss resulted in less complete records. The general character of the 
cores coincided satisfactorily with the western area as did natural exposures of marble where the formation 
exceeded 150 feet in thickness. Thinning of the formation naturally disrupted correlation procedures. 

Accurate information concerning changes in the various zones by thickening is not available, but it 
has been found that with a constant formational thickness the zones thicken and thin at the expense of each 
other, and that where talc replaces much of the white marble zone, the mottled zone is usually thinner and 
contains more tremolite and talc partings. 

It is important to note that the white, talc-bearing zone is in nearly the exact stratigraphic center of 
the marble. It is, therefore, in the geographic center of the marble belt unless wide variations in overburden 
or surface topography alter its relationship to contact lines. Utilization of these relationships in the search 
for talc is explained in the section on exploration procedure. Although other zones of the marble have more 
or less quartz in conjunction with slaty and actinolitic phases stratigraphically above the talc, the central 
white zone seems originally to have had sandy material as an impurity in otherwise pure dolomitic lime- 
stone. Principally quartz, but having small quantities of rutile and zircon, the sand exhibits the roundness 
and equant grains of typical beach or shelf deposits. Such conditions, though curious, are not irreconcil- 
able in view of the dolomitic character of the marble and in view of similar conditions which exist in 
Miocene marls of the Coastal Plain region of North Carolina : Twenhofel points out that many dolomitic 
sediments may represent shallower water conditions than do some of the purer lime sediments 1 ; Stuckey 
reports conditions wherein Miocene marls contain up to 30 percent silica, mostly in the form of rounded 
quartz grains 1 '. The sand possibly is introduced by a rolling of the grains along the basin floor rather than 
by a washing in of bulk material. At any rate, it is believed that the original sandy nature of the central 
marble zone was partly responsible (together with the dolomitic character) for the development of frac- 
tures in the marble, since the sand grains would assist in reducing the effectiveness of flowage, and these 
fractures permitted the entry of later solutions which silicified part of the marble and later formed the talc 


As a separation between the Murphy marble and the Nottely quartzite, this formation (mapped by 
Keith as the northwest limb of the synclinally folded Andrews schist :i ) is present throughout nearly the length 
of the Murphy marble belt in North Carolina, but any one description does not suffice in all localities. From 
Valleytown to Ranger, the formation comprises brown, coarse ottrelite schist with smaller but uniform 
amounts of pyrite. The ottrelite crystals range up to three-eighths inch in size and usually are at an angle 
to foliation and bedding. Pyrite occurs as aggregates of minute crystals both in the mass and aligned in 
the cleavage. Most characteristic of the ottrelite schist is the formation of brown limonite crusts and beds 
in the residuum as weathering takes place. Gradation of the schist into the Murphy marble is broad and 
relatively smooth so that nearly half of the formation is calcareous. Transition into the Nottely quartzite 
is more irregular but no less certain. Variations in total thickness range from 200 feet to about 450 feet. 

Northeastward from Valleytown and southwestward from Ranger, the ottrelite content decreases, both 
in size and quantity of the crystals, until a simple, finer-grained mica schist results and brown iron beds 
no longer are present. Except for stratigraphic position, this phase is nearly identical to the mica schist 
(ms) which lies just northwest of the marble. 

l W. H. Twenhofel, Treatise on Sedimentation. 2nd Ed., p. 34G, 1932. 

2 J. L. Stuckey, Personal Communication, 1947. 

3 Arthur Keith, 1907. 

14 Talc Deposits of the Murphy Marble Belt 

Internal structures in this formation are similar to the structures in schists and gneisses previously 
described. A notable addition is the crenulation of primary cleavage planes and the development of frac- 
ture cleavage along the axial planes of the crenulations, parallel to minor fold axes. Slickenside striae are 
not so apparent and lineations other than crenulation axes are less noticeable. 


As with the Murphy marble, the terminology of Arthur Keith is followed in denoting this formation 
since it is both characteristic and well-known by workers in the area. A part of Keith's description is quoted 
because it is in accord with present findings : 

. . . The formation consists entirely of white quartzite. As a rule, the shapes of the original 
grains of sand forming the rock are not visible except under a microscope. By that means (i.e 
the microscope) the original nature of the grains and their growth during metamorphism can 
be discerned. In some of the weathered outcrops and fragments the original form of the grains 
is again brought out when the secondary quartz has been dissolved away. Besides the quartz, 
a very small proportion of feldspathic material is usually present. Much of this was replaced 
by secondary quartz and muscovite during alteration of the rock. These latter minerals are 
now rudely parallel to the planes along which the motion took place in the rock. The schistose 
character thus introduced is strongest along the layers which originally were argillaceous or 
feldspathic. In some places the mica flakes become coarse and the rock approaches a quartz 
schist in appearance. As a rule, however, the quartzite is very fine-grained and glossy and is 
always white. . . . x 

Only one major correction of Keith's description is required. The Nottely quartzite does not consist 
entirely of quartzite, due both to the presence of quartz schist layers and to beds which are nearly identical 
to the adjacent ottrelite schist. Also, in a bluff overlooking Valley River, about 100 feet upstream from the 
Southern Railway bridge in the town of Murphy, a two foot bed of marble was found in the quartzite. 

Keith did not recognize the presence of the Nottely quartzite throughout the extent shown on the accom- 
panying geologic map, but showed it as being faulted out in most places northeast of Tomotla. He stated 
that a white quartizite lay in contact with the marble at several places near Topton and Hewitt, but noted 
it as faulted Tusquitee quartzite. While the Nottely quartzite, as here used, certainly is not seen every- 
where along its strike, it crops out at intervals close enough to warrant mapping as a continuous formation, 
and its stratigraphic and geographic position deny previous interpretations. East of Andrews it appears 
on the surface both as a hard, dense quartzite and as a mass of fine, white powder. Its termination at 
Hewitt may be explained partly by depositional conditions and partly by uncertain observations in difficult 
terrain. The nature of the Nottely formation has an important bearing on the Murphy marble. Further 
considerations are discussed in the description of the marble and of the general geologic structure of the 


These rocks are similar to the ottrelite schist (os) and were considered a part of the same formation 
(Andrews schist) by Keith. The formation is principally brown, pyritic, ottrelite gneiss, generally siliceous, 
with phases of ottrelite schist and feldspathic quartzite. Also contained in at least two localities are diorite 
sills up to 40 feet thick. These are near the eastern city limits of Murphy and at Caney Creek, three miles 
southwest of Murphy. "Pseudodiorite" is found in the gneiss in small quantities. Weathering of the ottre- 
lite gneiss produces beds of limonite in the residuum, resulting in the best known brown iron ores of Chero- 
kee County.- Ottrelite has been found altered to vermiculite, but not in commercial quantities. Between 
Tomotla and Andrews, where the Nottely quartzite is indistinct, wide gradations back and forth between the 
two formations are likely. In manner similar to the ottrelite schist, ottrelite decreases in quantity along 
the strike southwest of Ranger and northeast of Andrews, giving way to mica schist and quartz schist. 

Bedding, major and minor flow cleavages, fracture cleavage, and crenulations may be distinguished in 
most places, and a lineation of cleavage intersections parallel to fold axes is noticeable. In some of the 
quartzite beds a kind of boudinage structure shows elongation along the dip of the beds, but exposures 
were insufficient to allow acceptable measurements. 

Arthur Keith, 1007. 
W. S. Bayley, op. cit. 

Talc Deposits op the Murphy Marble Belt 15 


This formation is a part of what Keith mapped as the southeast limb of the synclinally folded Valley- 
town formation. Variations in lithology along the strike probably are more complex than in any of the 
other formations of the area. From Murphy to near Andrews, it is an ordinary staurolite-mica schist with 
zones of simple mica schist, dark micaceous quartzite and arkosic quartzite. Elsewhere the formation is 
barely distinguishable from the quartz-mica schist (qms) as it changes to chloritic and sericitic schist south- 
west of Murphy and to quartz schist, mica schist, and mica slate northeast of Andrews. Commercial flag- 
stone has been quarried and sold on a small scale near Valleytown. Ottrelite, biotite, chlorite, hornblende, 
and secondary muscovite and quartz are accessory minerals. 

Broad folding and (probably severe) faulting are in evidence, particularly in the vicinity of Marble and 
Andrews where shearing obliterates other internal structures at times. Interpretations of attitude were 
made possible by crenulations, occasional evidences of cleavage intersections, and a few small, more resistant 
quartzite beds. 


This series has not been mapped in its entirety because of its wide extent and remoteness from the talc- 
bearing marble, although studies were made in the vicinity of the Peachtree and Martins Creek marble 
localities. It is a series of quartz-mica schist and intermittent zones that probably represent original quartz- 
ites which resisted shearing action. Eastward from Topton, the rocks gradually become more dense and 
less schistose, with beds of massive quartzite becoming more prominent. Colors are light brown to dark 
gray. Much of the rock exhibits a characteristic "brassy" sheen on exposed dip surfaces, prompting the 
name Brasstown for the settlement after which Keith named his equivalent formation. 

In his Brasstown formation Arthur Keith recognized lithologic variations which could not be attributed 
entirely to folding, and it is easy to interpret his description as that of a series rather than a formation. 
However, much of the rocks previously mapped as Tusquitee quartzite are now believed to be stratigraph- 
ically separated facies or remnants within the quartz-mica schist. The entire series appears to be a zone 
of thrust faulting at, or near, an anticlinal axis, though it has not been possible to determine the prevailing 
attitude of bedding because of strong foliation which more or less parallels the generally steep, southeast- 
ward-dipping beds. 

DiORITE (do) 

Igneous rocks in the Murphy marble belt and surrounding areas have received little notice from geolo- 
gists in the past. LaForge and Phalen 1 and Emmons and Laney 2 briefly mentioned gabbro dikes from the 
Ducktown copper area, and field workers have noted smaller but similar exposures near Bryson City, Swain 
County, North Carolina. Local workers have also recognized a large diorite dike or sill, similar to those de- 
scribed herein, in the vicinity of the Fontana and Adams Copper Mines in Graham County, North Carolina. 
A somewhat different type of igneous-appearing rock, "pseudodiorite," has received attention in geologic 
literature and is described later. 

Current work has revealed for the first time 3 the nature and extent of a series of diorite sills which 
occur about 300 feet to 450 feet stratigraphically above and below the Murphy marble. Exposures have been 
found northwest of the marble near Hewitt and at Kinsey, and southeast of the marble at the eastern city 
limits of Murphy and on Caney Creek three miles southwest of Murphy. The rock has the same general 
appearance in all localities, being of dark gray-green color, granitic to porphyritic texture, and showing 
varying degrees of alteration. The term diorite is used advisedly, but there is so little feldspar showing 
that the rocks might be termed pyroxenite and amphibolite. The lack of feldspar and quartz, however, may 
be due to alteration by later solutions, and the term "metadiorite" might be preferable. Marked schistosity 

'Laurence LaForge and W. C. Phalen, U. S. Geol. Survey, Geol. Atlas, Ellijay Folio, no. 187, 1913. 

2 W. H. Emmons and F. B. Laney, U. S. Geol. Survey, Prof. Paper 139, Geology and Ore Deposits of the Ducktown Mining District, 

3 The TVA Geologic Division has on file a thin section (No. 42) of "uralite schist" collected from near Kinsey. but the present 

writer was not able to re-establish the field locality. 


Talc Deposits of the Murphy Marble Belt 

is seldom present, although secondary chlorite, biotite and quartz cause a platy appearance in some places, 
and altered mica schist in the contact zones may be mistaken for sheared diorite. 

Just east of Hewitt a diorite sill, about 40 feet thick, has been traced for 'about two miles along the 
mica schist and quartz-mica gneiss contact (Fig. 3). Strike and dip appear to conform with the country 
rock throughout. The rock has a fine groundmass of chlorite and biotite with more or less quartz, mus- 
covite, and feldspar. Phenocrysts are light-green actinolite and darker uralit£. Under the microscope, 
zircon and tourmaline were found and the feldspar was identified as andesine. Contact metamorphism is 
not evident by megascopic examination but petrographic studies of adjacent rocks reveal chlorite, zircon, 
zoisite, hornblende, and pyroxene. 

At Halls Ford, near Kinsey, six miles southwest of Murphy, a sill measuring 38 feet in thickness has 
been traced across a big bend of the Nottely River for about one mile, following the contact of the mica 
schist and the quartz-mica gneiss. Outcrops range in size from a few feet to blocks 15 feet high and 20 feet 
wide. It is difficult to distinguish the rock from quartzite except by close inspection, although occasional 
outcrops exhibit peculiarly irregular surfaces upon weathering (Fig. 4). Certain small zones have a high 
carbonate content, and they weather like limestone or marble. Unoriented phenocrysts of actinolite are up 

Fig. 3 — Diorite (Between the Figure and the Camera) , on the South- 
ern Railroad, Pole No. 2331, 1.7 Miles East of Hewitt. Look- 
ing South. 

to three-eighths inch long, being larger than in the sill near Hewitt. Petrographic study of two specimens 
did not reveal any feldspar or quartz in the fine ground mass of chlorite and muscovite. Schistosity is poorly 
developed and bedding is not visible so the dip and strike could not be measured on the ground. Adjacent 
rocks are too deeply weathered to allow determinations of contact metamorphism or transition into the coun- 
try rock. 

Southeast of the Murphy marble, near the contact between ottrelite gneiss and staurolite-mica schist, 
evidences of sills are less certain. At the Murphy Cannery, just north of U. S. Highway 19 at the eastern 
city limits, a dark-green dioritic or gabbroic rock may be seen within ottrelite gneiss. Hornblende and 
actinolite crystals occur in a quartz-chlorite-feldspar groundmass with a few pale pink garnets, and small 
inclusions of ottrelite gneiss occur within the sill which seems to have a thickness of about 30 feet. The 
rock is dense and hard since the small amount of chlorite and excess of quartz is not conducive to the platy 
nature of similar exposures elsewhere in the area. Scarcity of outcrops necessitated mapping mostly on 
the basis of float and altered schist, and the accompanying geologic map shows an extent of less than 2,000 

Talc Deposits of the Murphy MaPvBle Belt 


Fig. 4. — Diorite on Right Bank of Nottely River at Halls Ford, Near 
Map Location No. 5. Looking Southwest. 

Diorite outcrops and float have been mapped for about 4,000 feet near the mouth of Caney Creek south- 
west of Murphy. Best exposures are in the creek bed and bank and in a borrow pit on the south side of U. S. 
Highway 64. The petrography is similar to that of the Kinsey sill, showing no feldspar, little quartz, and 
a few small specks of manganese oxide. 

Some indications of the structure of the sills already have been given. Little or no schistosity is appar- 
ent, attitude seems to conform with the country rock, and systematic joints are absent. Because of difficulty 
in recognizing the existence of these rocks, it is not improbable that other exposures will be found in the 
future along the two contact lines. It is certain, however, that the sills are discontinuous along the strike 
and probably along the dip as well. The fact that the sills have been found in the same stratigraphic posi- 
tion over a distance of nearly 35 miles is indicative of possible fault plane control. 

In addition to these large, well-defined igneous sills, mention has been made of gabbroid dikes or sills 
which are present in the phyllites to the northwest. They range from a few inches to at least four feet in 
thickness and have been measured up to 20 feet along the dip, but they have not been recognized along the 
strike. They are similar to gabbro dikes in the Ducktown region and nearly identical to gabbros in Keith's 
Nantahala slates on the Tuckaseegee River below Bryson City. Large augite and uralite crystals are set 
at random in a groundmass of very fine quartz with smaller amounts of chlorite and brown biotite. Colors 
range from dark brown to greenish-black. Schistosity is almost entirely absent and the rock is so tough as 

18 Talc Deposits of the Murphy Marble Belt 

to firmly resist breaking with a pick. Ordinarily the intrusives are parallel to steeply dipping beds, but 
they have been found pushed up in the centers of small anticlines. Because of their small size, no attempt 
has been made to show these rocks on the accompanying geologic map. 

Direct evidences of rare or commercial minerals have not been found associated with these various 
types of igneous rocks, though indications of them may show up in representative chemical analyses. It 
seems probable that these rocks are inter-related with late alterations of the rocke of the area (formation 
of late quartz, muscovite, chlorite, biotite, amphiboles, pyrite, phlogopite, etc.), with the formation of 
"pseudodiorite," and finally with the formation of talc deposits. These factors will be considered later in 
discussions of the talc. 


Not to be confused with the above mentioned diorites and gabbros are small nodules and stringers of 
a light-colored, igneous-appearing rock which Keith originally called quartz diorite dikes 1 and later called 
pseudodiorite 2 . Other writers have added to Keith's descriptions 3 . Briefly, the rock is a white quartz-feld- 
spar groundmass with both oriented and unoriented metacrysts of hornblende and garnet, together with 
occasional biotite and calcite. Varied degrees of zoning usually exist as hornblende metacrysts become 
smaller and more numerous toward the outer edges of the bodies. Most of the formations other than the 
Murphy marble and the dense white quartzites contain some "pseudodiorite." 


In the area of the Murphy marble belt, dock weathering and the transportation of weathered debris are 
dependent on geologic structure nearly as much as on rock composition. Coarse, schistose rocks are usually 
more resistant to chemical decomposition than many other types, possibly because percolating ground 
waters move faster in the schists and do not have time to attain heavy concentrations of corrosive agents. 
In consequence, coarse schists are commonly found to have a minimum average thickness of overburden. 
Very dense, hard quartzite is the most resistant of all rocks in the area, but slight increases of structural 
weakness and of easily weathered minerals result in fairly deep overburden. Gneisses and fine-grained 
schists are most susceptible to weathering, and they usually have the deepest residual mantle. Pure marble, 
when fractured, is attacked by ground waters and dissolved with comparative rapidity, but all material is 
carried away and no residuum remains in place. As the percentage of impurities in marble increases, 
weathering characteristics become more nearly like those in other types of rocks and some form of residuum 
may be formed. 

Specifically, experience has shown that in localities where talc exploration and mining are carried on 
along the Murphy marble, the thickness and type of overburden varies more or less with elevation. In low 
valley bottoms, the marble is covered by from 5 to 20 feet of silt, sand, gravel, and small and large boulders. 
Overburden ranges from 20 feet to 80 feet on the higher benches and sides of valleys, and contains fewer 
boulders and thicker sands and clays. On higher benches and in the gaps, total overburden may be as 
much as 130 feet, usually averaging 60 feet to 80 feet. Top gravels and boulders are rare except along the 
Nantahala Gorge, and float of the Nottely quartzite is not abundant enough to cause difficulty in core drill- 
ing work. 



The general character of original sedimentation in the southern Appalachians has long involved ideas 
of rapid erosion and rapid deposition in irregular, discontinuous basins. For example, if one pictures the 
conditions under which deposits are being formed today along our southeastern coastline, with its sinuous 

1 Arthur Keith, 1907. 

2 Arthur Keith, Production of Apparent Diorite by Metamorphism, Geol. Soc. Am. Bull., vol. 24, pp. 684-685, 1913. 
1 Laurence LaForge and W. C. Phalen, op. cit. 

W. H. Emmons and P. B. Laney, op. cit. 

C. S. Ross, Origin of the Copper Deposits of the Ducktown Type in the Southern Apalachian Region, U. S. Geol. Surv., Prof. Paper 

179, 1935. 

B. C. Moneymaker, Character of the Great Smoky Formation in the Hiwassee River Basin of Tennessee and North Carolina, Tenn. 

Acad. Sci., vol. 13, no. 4, pp. 291-93, 1938. 

Talc Deposits op the Murphy Marble Belt 


inlets, sounds, bars, peninsulas, and islands, and if one further pictures cyclic ingress and egress of the 
sea, the complex possibilities of gradation and hiatus are apparent. Imagine these calcareous deposits, sands, 
and silts being solidified, pushed up, crumpled, sheared, and partly eroded ; such processes are involved in 
the geologic history of our present inland rock formations. In the vicinity of the Murphy marble belt, con- 
glomerates, quartzites, gneisses, schists, and marble show intergradation, and their relations to each other 
are affected by folding and fracturing and by the injection of hot, aqueous liquids and vapors derived from 
underlying igneous masses. With these conditions in mind local changes along and across the strike of 
formations can be explained. 


In his mapping of the Nantahala quadrangle 1 , Keith concluded that the Murphy marble and adjacent 
formations were part of a broad syncline in which the marble was prevented by faulting from reappearing 
southeast of the fold axis. It seems likely that much of Keith's theory was based on the outcrop patterns 
of folds in the Murphy marble and on the idea that all folds plunged to the southwest, thus requiring a 
synclinal structure as the only logical interpretation if his data were sufficient. 

Between Culberson and Andrews, a study of cleavages northwest of the Murphy marble shows with 
little doubt that southeast-dipping beds are overturned, except in the minor folds, in all rocks from the 
phyllite and mica schist (pms) to the mica schist (ms). Similar studies at Murphy indicate overturning in 
the ottrelite schist (os) and ottrelite gneiss (og). Although few internal structures of the Murphy marble 
point conclusively to overturning, features that might characterize overturned beds have been recorded 
inadvertently as far back as the work 2 of Loughlin, Berry, and Cushman (See Fig. 5). 



1 ^VIM 

^\ VjM 

Fig. 5. — Sketches Showing Internal Fractures in Marble from Regal 
Quarry (after Loughlin, Berry and Cushman). Arrows Have 
Been Added to Show Relative Movement and Possible Indica- 
tions of Overturning. Anticlines Would be in Direction of 
Hanging-wall Sides. 

The presence of overturned southeast-dipping beds over such a broad area can be explained satisfac- 
torily by assuming them to be part of the northwest limb of an overturned anticline. Further evidence of 
anticlinal structure is seen by comparing the outcrop pattern of northeast-plunging folds with the pattern 
of southwest-plunging folds in the Murphy marble (See Geologic Map). A blanketing schistosity ren- 
ders cleavage analysis undependable in most of the rocks southeast of the marble belt, but a few indica- 
tions of normal stratigraphic sequence have been found in the quartz-mica schist (qms). This might lead 

1 Arthur Keith, 1907. 

2 G. F. Loughlin, E. W. Berry, and J. A. Cushman, op. cit., pp. 38-39. 

20 Talc Deposits of the Murphy Marble Belt 

to the assumption, which requires confirmation by additional study, that the Peachtree-Martins Creek marble 
is a part of the southeast limb of the anticline. 

Dip and strike vary from place to place along the Murphy marble belt, but for estimating and project- 
ing purposes it is convenient to use N45°E for the strike and 50°SE for the dip. Bedding is often parallel 
to schistosity but deviation may occur in a critical locality. The most accurate criteria for bedding deter- 
minations are banding and facies changes, and all other criteria should be regarded with suspicion, but 
even banding might be caused by non-conforming structures. The most satisfactory method is to compare 
several criteria and check one against another. 


References to minor faults have already been made in the preceding discussion. Fault planes that show 
considerable movement have not been observed directly, but drag structures indicate that such faults do 
exist near some of the minor folds in schistose and gneissic rocks. In connection with rocks of the Great 
Smoky and Hiwassee formations, where structures are of the same age and general type as are those along 
the Murphy marble belt, the writer has reported that normal fault zones having dip slips of up to 200 feet 
measured in tenths of feet in width, whereas thrust faults having little slip exhibited shear zones of ten feet 
or more 1 . Similar conditions should be expected in rocks adjacent to the marble. 

As was disclosed in the section on folds, stratigraphic interpretations do not require postulation of the 
Murphy fault 2 , nor are the faults of the Stoses 3 necessary to an explanation of the position of the Murphy 
marble-Andrews schist-Nottely quartzite group of rocks. If these faults are non-existent, the Murphy 
marble is a part of the Ocoee series and is older than either the Great Smoky formation or the Nantahala 
slate. The failure of the marble to reappear northwest of its present outcrop is not incongruous, because 
it is probable that original conditions of sedimentation did not allow calcareous sediments to extend very 
far along the dip. As has been noted, however, a very great amount of stress has been relieved throughout 
the mica schist (ms), staurolite-mica schist (stm), and quartz-mica schist (qms), and hundreds of feet of 
displacement could be represented in any of these formations. It is believed that the actual amount of 
displacement cannot be determined until many additional detailed studies have been made along the trend 
of these formations. 


The fractures produced by dynamic metamorphism are controlled, in part, by the relative competency 
of the rocks involved. Relative competency varies in turn as metamorphism progresses, so that older frac- 
tures influence fractures which are formed at a later time. A stress which is applied slowly in coarse, 
crystalline marble can be relieved, without fracture, by a gliding along internal planes of individual crystals 
and a subsequent recrystallization of the marble. A number of conditions indicate that such an action has 
taken place in a part of the Murphy marble: pure, coarse phases of the marble are relatively free from 
fractures even though differential movement must have taken place ; fine-grained dolomite and impure mar- 
ble, however, was less capable of rescrystallization and, therefore, susceptible to fracturing which gave access 
to mineralizing agents. These conditions have a direct bearing on the size and position of talc deposits. 

Flow cleavage and fracture cleavage are foliate structures which are of prime importance in the Murphy 
marble belt. Flow cleavage is present in beds of incompetent micaceous rocks, and nearly parallels the 
limbs of folds. Fracture cleavage is an equivalent structure of the denser, more competent quartzites and 
marble and is more nearly perpendicular to the limbs of folds. Both cleavages may be used, with a few 
exceptions, to determine whether the rocks in which they occur are overturned or in a normal position. The 
acute angle of intersection of cleavage and bedding will point in a direction which, if followed along the bed- 
ding, leads to the crest of an anticline (Fig. 6). Cleavages provide paths for mineralizing agents and are 
common locations of secondary minerals. 

All rocks in the area of the Murphy marble belt exhibit a more or less common regional foliation termed 
schistosity. Secondary fractures were formed during the later stages of metamorphism, and these new 

1 Unpublished TVA report, Geology of the Apalachia (dam and tunnel) Project, May 1943. 

2 Arthur Keith, 1907. 

3 G. W. and Anna J. Stose, 1944. 

Talc Deposits of the Murphy Marble Belt 


fractures attempted to follow the cleavages which had been formed previously. Thus, the schistosity is 
a special combination of flow cleavage and fracture cleavage. The schistosity usually has a steep southeast 
dip, roughly parallel to bedding except where minor folds cause bedding planes to vary while the schistosity 
continues unchanged. Movement along the planes of schistosity is reflected in striae or grooves from a frac- 
tion of an inch up to two or three inches across. Schistosity is less severe in dense quartzites and nearly 
absent in the marble, but incipient weaknesses are revealed where secondary mica and other platy or acicu- 
lar minerals have been formed. 

A great deal of the stress imposed on rocks of the area has been relieved by foliation in the schists and 
gneisses, and extensive joint systems are prominent only in more competent quartzites and in fine-grained, 
dolomitic phases of the marble. Joints do not extend for long distances, nor do joint systems seem to have 
very distinctive orientation, although it is likely that trends might be revealed if many hundreds of joints 

Fig. 6. — Schematic Cross-Section Showing Relation of Cleavages to 
Folds in Competent (C) and Incompetent (I) Rocks. Arrows 
Indicate Direction of Relative Movement Along Bedding. 

were plotted on polar nets. Subsequent movement is apparent in many joints of the area and innumerable 
comparative age groups of joints are represented. Because of the manner in which planes of foliation and 
bedding are interconnected by joints, percolating ground water has greater penetration and more readily 
weathers the country rock. 


The term "lineation" can be applied to various types of linear phenomena in rocks, such as fold axes, 
striae, flow lines, elongations and intersections. The cleavages described above appear as lineations when 
they are seen in section only as a single line or group of parallel lines. Lineations may be denoted by their 
pitch, which is measured by protraction from the horizontal within the plane on which the lines are seen, 
or, more simply, by their plunge, which is measured from the horizontal by means of a clinometer, in the 
vertical plane that includes the bearing of the plunging line. Carefully weighted results of lineation studies 
are helpful in deciphering geologic structures, since lineation is controlled by movements which have taken 
place, with particular reference to axial planes of folds. 

Slickenside striations form one class of lineation that occurs widely in this area. The striae usually 
plunge southwest on planes of schistosity but sometimes have other directions of plunge on joints, bedding 
planes, and small faults. Easily confused with thesestriae are lineations formed by the intersection of 
cleavages, where the trace of one cleavage plane shows on another as a tiny ridge or crack. The direction 
of plunge of cleavage intersections on schistosity planes has been demonstrated to correspond to the plunge 
of minor folds along the Murphy marble belt, allowing structural interpretations which have been obscur- 
ed heretofore. In the present work, it has been found that talc bodies of the area also plunge in accord with 
cleavage intersections, as do many other types of ore bodies in the southern Appalachian region. 

22 Talc Deposits of the Murphy Marble Belt 

In the ottrelite gneiss, southeast of the Notteley quartzite, a form of lineation known as boudinage has 
been observed in several exposures, particularly in a road cut opposite the Murphy cannery. Stretching 
parallel to fold axes appears to have pulled siliceous rocks apart by tension, resulting in separated blocks 
which are elongated parallel to fold axes. One other form of lineation is represented in conglomerate 
beds of the Great Smoky formation at Mill Dam, three miles northwest of Murphy, where maximum elonga- 
tion of stretched pebbles is approximately parallel to fold axes. « 



In the section on zoning of the Murphy marble, it was pointed out that the approximate stratigraphic 
center of the formation is occupied by a fine-grained, white, dolomitic marble which sometimes contains 
talc deposits. Many dozens of observations show without exception that talc bodies of any commercial size 
are not found outside this central zone. Other portions of the marble contain talc in the form of scales, 
partings, and small pockets, and certain slaty zones near the northwest contact of the marble are talcose, 
but these cannot be termed talc deposits. Reports that talc occurs near the marble contacts have been based 
on the position of talc which later was proved to have been moved by slumping and creeping. Other erron- 
eous data have resulted from concentration of originally disseminated talc scales or of minor quantities of 
tremolite which has been altered to talc. Caution must be exercised when attempting to correlate the occur- 
rence of talc in localities where the Murphy marble formation is extremely thin and composed mostly of 
quartz and micaceous material. These conditions are analyzed in the section dealing with the marble 


Configuration of the Bodies — The lenticular tendency of talc bodies in the Murphy marble has been 
recognized at least since the report of J. H. Pratt in 1900 1 , and recent investigations have convinced the 
writer that all talc bodies of commercial size are roughly lens-shaped. Indications are that these lenticular 
bodies have echelon arrangement, with a "line of bearing" parallel to the strike of the marble in which 
individual lenses vary from the local strike in amounts depending upon the degree of plunge (Fig. 12). 
Lenses that have been discovered thus far plunge either northeast or southwest at an average angle of about 
18° from horizontal, varying from zero to as much as 35°. Dimensional ratios of the talc bodies could be 
used to good advantage in explorational work, but extreme variations render valueless any theoretical fixed 
ratios other than to say that strike length is greater than thickness or breadth. Actual "pinching out" of 
the talc in any direction may occur by fingering, transition, or breaking up into smaller isolated bodies, 
although experience has shown that the presence of marble inclusions in the main body can be mistaken 
for "pinch-out" warnings. 

Controlling Structures — In the sections Zoning in the Murphy Marble and Cleavages and Joints, it was 
pointed out that the central talc-bearing zone of the marble is dolomitic and especially liable to fracturing. 
Since the attitudes of talc bodies are known to coincide with foliate structures, and since it is doubtful 
that the structures are of post-talc age, it might be assumed that both the attitudes and shapes of the talc 
bodies result from similar attitudes and shapes of fracture systems. 

In order to explain the lenticular nature of the talc bodies, it must be realized that rock deformation 
seldom results from uni-directional forces, but rather from multi-directional forces which twist and either 
compress or pull apart. Fracture systems, like folds and lineations, attain plunging attitudes by the in- 
fluence of later unbalanced (e.g. tilting) forces, and as fracture systems must have spatial limits, it is nat- 
ural that they exhibit gradations in severity. Thus, a fracture system can be so deformed that it attains an 
ellipsoidal outline within which the individual openings are large near the center of the system and non- 
existent beyond the outer edges. If other suitable mineralizing conditions exist simultaneously or sub- 
sequently, mineral deposits may be formed in, or controlled by, these three-dimensional zones of weakness. 

In summary, the talc deposits have their present shapes and attitudes because the action of complex 
forces resulted in simple, ellipsoidal systems of weakness which controlled the travel of talc-forming agents. 

1 J. H. Piatt, op. cit. 

Talc Deposits of the Murphy Marble Belt 23 

Internal Structures — The various talc deposits have internal structures which differ from place to place 
only in degree and direction. Common to nearly all of the talc, and parallel to regional schistosity, is a min- 
utely spaced cleavage which gives the talc a fibrous or foliated nature. The origin of this cleavage is ob- 
scure, although several possible explanations can be advanced. One possibility is that the talc might have 
replaced schistose marble in such a manner that the original foliation pattern was reproduced much as grain 
is reproduced in petrified wood. Objections to this theory are that foliation is stronger in the talc than in 
adjacent marble, and, in addition, slickenside striae are present in the talc but are seldom found in nearby 
marble. The explanation favored by the writer assumes that talc formation took place during a lull in 
rock deformation near the end of the last great period of metamorphism (Carboniferous age) and that only 
slight movement occurred after the talc was in place. The theory allows for those few examples of massive 
talc which are known to exist (principally at Hewitt) and conforms to observed data which have been de- 
rived from studies of certain other mineral deposits and igneous intrusions. It certainly does not seem prob- 
able that the talc could be in its present condition if it had been subjected to the full force of movements 
which caused regional schistosity. 

Although joints are present in talc bodies, they are, for the most part, younger than any of the other 
structures, and seldom pass into the surrounding marble. Intervals between joints are rather wide, at 
least several feet. Excepting movement that has taken place along the foliation, few important faults are 
found in the talc. One irregular normal fault of unknown displacement occurs in the Nancy Jordan Mine. 
It strikes nearly 45° from the principal foliation and dips vertically. In talc bodies which have distinct foot- 
walls and hangingwalls, movement seems to have occurred along the walls approximately parallel to the 
local direction of plunge. Lineations of cleavage intersections may be seen on planes of the principal folia- 
tion and occasionally on footwalls and hangingwalls. These lineations are always parallel to the local trend 
of the talc body's long axis. 

One type of internal structure that has not been explained satisfactorily is a kind of roll around the 
longitudinal axis of the talc lens. Rolls occur on both footwall and hangingwall and are the means by 
which the talc thins and thickens along the dip. At the Mulberry Gap Mine, the hangingwall has a fairly 
constant dip but the footwall undulates. At the Nancy Jordan Mine both walls have rolls, and similar con- 
ditions exist at the Carolina Mine. In most of the currently accessible talc pits and adits at Hewitt, rolls 
are confined mostly to the hangingwall. 


The average grade of commercial talc in the Murphy marble is of high quality as compared to talc from 
other parts of the country. One set of weighted averages, derived from data of the U. S. Bureau of Mines 1 , 
indicates total impurities amounting to less than four per cent. Impurities noted in those samples were 
ferrous iron, carbonates of calcium and magnesium, rutile, zircon, and epidote. Other minerals which 
have been observed from time to time include tourmaline, garnet, monazite (a single grain), muscovite, 
chlorite, phlogopite, pyrite, magnetite, amphibole, zoisite, scapolite, and serpentine ( ?) . Of these minerals, 
talc, quartz, amphibole and carbonate are associated the most intimately. 

The following descriptions of minerals are based on megascopic observations supplemented by petro- 
graphic studies. Unfortunately, sampling for petrographic work was erratic. Most specimens were col- 
lected early in the program in search of criteria which might be used to predict the location of talc bodies 
along the strike. Nearly all talc-quartz specimens are from a common horizon (bottom) of the talc. Com- 
plete chemical analyses of talc from the different deposits have not been made recently, but several older 
analyses are available. 

Talc — The color of the fresh talc varies from pure white (equal to standard magnesium carbonate) 
through greenish-white, green, blue, and gray. Variation in color may be due in part to the refraction of 
light through minute fracture systems. All of the talc is fibrous to some extent, although at Hewitt some 
varieties have most of the properties of massive talc. Fibrous structure does not prevent the talc from 
having good strength when cut into crayons, and large talc blocks can withstand severe treatment without 

l U. S. Bureau of Mines: Survey of the Suitability of Domestic Talcs for High-Frequency Insulators, R. I. 3S04. April 1045. 

24 Talc Deposits of the Murphy Marble Belt 

breaking down. In the vicinity of hangingwalls and footwalls, it is not unusual to find very hard glazed 
talc with the grain curved on short radii. In this connection it should be explained that footwalls and hang- 
ingwalls do not delimit the occurrence of talc. A mixture of talc and marble or talc and quartz continues 
for a few inches or even feet beyond the walls. 

The petrography of the talc appears to be rather complex. Some thin-sections of pure talc show a 
marked orientation of elongate talc, while others show little uniformity as reflected in extinction positions. 
Talc has been observed to replace tremolite, quartz, carbonates, muscovite, phlogopite, and various heavy 
minerals, and it has been found to follow cleavage planes between individual minerals without alteration 
of either talc or accessories. Large unaltered crystals of tourmaline and tremolite have been found imbed- 
ded in talc, and there are indications that talc may have been replaced at times by muscovite, clinozoisite, 
and apatite. Where talc occurs as disseminated scales and partings outside the main talc zone, little evi- 
dence of replacement can be seen, and it is possible that the talc is merely an interstitial filling or, at most, 
a replacement of equally thin fillings of secondary quartz or mica. 

In the large talc bodies the transition from talc to marble and /or quartz is gradational. Smaller iso- 
lated talc pockets and fingers have rims of mixed talc and wall rock, and "footwalls" and "hangingwalls" 
do not cause sharp contacts. On the other hand, changes in the quality of talc within a single body tend 
to be abrupt, and contacts between grades have plunges comparable to those of the parent masses of talc. 

Quartz — Three distinct types of quartz are contained in both the marble and the talc deposits. Vein 
quartz is the most rare and possibly the least important. Stuckey 1 reports the occurrence of probable vein 
quartz in dumps of the Hayes prospect (Location No. 20) at Tomotla, where large masses of cherty quartz 
show replacement by small quantities of tremolite and talc. 2 At Section Six (Location No. 13), the writer 
has found chunks of glassy quartz, twelve inches by four inches, which showed definite replacement by 
talc. Smaller quartz veins (up to one inch thick) have been seen in talc, marble, and silicified marble at 
the Mulberry Gap Mine. Definitely rounded detrital sand grains have been found in talc bodies and in silici- 
fied marble all along the Murphy marble belt from Hewitt well into Georgia. These grains are fairly rare 
in masses of pure talc in areas where the carbonate facies are reasonably thick, but they are more abundant 
where quartzitic and slaty facies begin to encroach. However, sand grains are quite noticeable near the 
outer edges of talc bodies where masses of silicified marble are adjacent to the talc. 

From time to time, references have been made to silicified marble almost as if it were a separate zone 
or rock type. Such an allusion is convenient and is probably not incorrect. The term refers to a rock, a 
part or all of which is quartz, that apparently once was marble. At the Mulberry Gap Mine, this siliceous 
rock attains a thickness of nearly 40 feet, and it is equally thick on the southwest side of Talc Mountain 
at Hewitt. In other places it is less thick and some talc bodies contain the rock in the form of nodules or 
"kidneys" from a few inches to several feet across. Studies of thin sections of the silicified marble indicate 
that some quartz individuals are definitely rounded and apparently detrital, while others are sub-rounded 
as if they had been partly resorbed. It is possible that some, but not necessarily all, of these rounded quartz 
grains are similar to those in the Gaffney (South Carolina) marble, where Kessler found a similar shape in 
quartz grains that blended into patchy aggregates. These aggregates in turn blended into definitely non- 
clastic quartz veinlets whose marginal grains had the same rounded outlines. 3 However, most of the quartz 
individuals in the silicified zone of the Murphy marble have irregular outlines and are grouped in homo- 
geneous masses suggesting hydrothermal origin. Lineation in the mass of the silicified marble is more 
apparent in hand specimens than in thin sections. Much of the quartz is replaced by talc directly and in 
other places the talc occurs along microscopic shears. The quartz is also replaced by tremolite, tourmaline, 
carbonates, phlogopite, muscovite, chlorite, zoisite, zircon, and pyrite, and it in turn replaced carbonate, 
muscovite, zircon, and possibly tremolite. 

Carbonate — Calcite and dolomite are important chiefly because they go to make up the marble which 
contains talc. Calcite is of further importance as an impurity, being undesirable in ceramic talc. Beyond 
the possibilities mentioned in the section on general geology, the original source of the marble is obscure 

1 J. L. Stuckey. Personal Communication. 194fi. 

-J. L. Stuckey, 1937. 

5 T. L. Kessler, Personal Communication, 1947. 

Talc Deposits of the Murphy Marble Belt 25 

and will not be discussed again. It is possible that secondary calcite has been introduced hydrothermally 
but a re-use of already available calcite can satisfy all the requirements needed in explaining phenomena of 
calcite occurrences. Dolomite is needed because it is possible that the talc deposits would not have been 
formed had not some (but not necessarily all) magnesia been already present. It has been observed that 
calcite is replaced by talc, quartz, tremolite, tourmaline, phlogopite, chlorite, muscovite, zoisite (or clino- 
zoisite?), zircon, and pyrite. Individual carbonate grains in the marble vary in size from sub-microscopic 
to nearly one-half inch, and comparisons with chemical analyses indicate the possibility that the finer- 
grained marble is more likely to have a high magnesia content. Two types of carbonate occurrences are 
present within talc bodies. The first is in the form of unaltered inclusions of marble (kidneys) which 
may be found distributed non-uniformly. The second type is in the form of vugs and veinlets of crystalline 
calcite which are encountered in only a few places, particularly near the edges of talc bodies. 

Amphibole — Stuckey 1 reports the occurrence of hornblende in the Murphy talc and all workers have men- 
tioned, with varying emphasis, the presence of tremolite and its iron-bearing relative, actinolite. Horn- 
blende in either the marble or talc has not been observed by the writer. Actinolite is widely distributed 
throughout the marble formation and usually is accompanied by pyrite. Commercial talc bodies rarely 
contain actinolite although the white (talc-bearing) marble zone may contain actinolite where talc is not 

Pratt- believed that most, if not all, of the Murphy talc resulted from an alteration of tremolite. While 
tremolite certainly alters to talc, the writer is doubtful that any talc deposits of commercial size are derived 
directly from tremolite. In the Murphy marble, tremolite is found in sizes from microscopic particles to 
bladed "crystals up to 20 inches long. It occurs as individuals and as oriented and unoriented aggregates in 
all parts of the marble formation. Tremolite replaces and is replaced by talc and most of the other accessory 
minerals, demonstrating several different stages of formation, but tremolite probably was never present in 
the quantities previously supposed. 

Although tremolite is intimately associated with talc, experience has shown that it is never abundant 
in and about the larger talc deposits, but often it is abundant within the central white marble zone when 
talc is not an important constituent of the rock. When tremolite replaces quartz or marble, it gives the illusion 
of sharp needles bodily piercing the invaded material 3 ; but when tremolite crystals are replaced by talc, it 
is not unusual for the talc to form as a broad encroaching wave. Tremolite is not a satisfactory criterion in 
the search for talc because it is present in so many parts of the marble. However, the writer has noted a 
marked increase of tremolite as drilling progressed along the strike away from known talc deposits. 

Other Minerals — Pyrite is distributed throughout every horizon of the Murphy marble, especially in the 
slaty, actinolitic, and mixed zones. It ranges in character from minute specks to cubes up to one inch 
across, and occurs as disseminated particles and as coatings on joint faces. Pyrite is least abundant in the 
talc and in white, fine-grained dolomite, although it is an important impurity in some of the talc in Georgia 
near the state line. Tourmaline occurs sometimes as the black, iron variety, schorl, and more often as the 
brown, magnesium variety, dravite. Dravite crystals, up to three inches long, have been found in silica 
zones separating talc from marble in the Nancy Jordan Mine and in mixtures of talc and tremolite at Maltby. 
Crystals of black tourmaline have been found in otherwise pure talc at the Mulberry Gap Mine, but these 
crystals seldom exceed one-quarter inch in length. The presence of tourmaline, together with magnetite, 
lend credence to theories of high temperature mineralizing conditions. Sericite and chlorite have been ob- 
served in many of the impure phases of the Murphy marble. Chlorite is seldom seen in association with 
large talc bodies, but sericite is rather common, especially in the gray "sheened" talc. 

Approximately 200 pounds of talc sawdust from one location was panned down, originally in search 
of magnetite. The panned concentrates of black sand amounted to about two tablespoonfulls, and exami- 
nations under the microscope disclosed well rounded grains of rutile, zircon, epidote, zoisite, garnet, ilmen- 
ite, magnetite, and a number of unidentified minerals, as well as quartz sand. Detrital heavy-mineral grains 
also have been found in thin sections, but, in addition, rutile, zoisite, zircon, and epidote of almost certain 
primary occurrence have been seen. 

1 J. L. Stuckey, 1937. 

2 J. H. Pratt, 1900. 
S J. L. Stuckey, 1937. 

26 Talc Deposits of the Murphy Marble Belt 

In drill cores where the white marble zone was intercepted without finding commercial talc, irregular 

masses of scapolite, about one inch across, have been identified. These possibly may have resulted from 

the alteration of feldspar fragments, or they might have a primary origin. Phlogopite usually is present 

in the scapolite localities and is not an unusual member of the outer zone around talc bodies and in the 

mixed and slaty marble zones. 


On the dumps of the Carolina Talc Company mine, near Kinsey, are fragments of a dark green, slate- 
like rock with greasy lustre and feel. The material is fairly soft and has many of the characteristics of 
serpentine, though identification under the microscope was not positive. The writer has not seen this ma- 
terial in place, but its occurrence on the talc "footwall" has been reported. 1 


Gillson notes that definite conclusions have not resulted from the numerous studies of the chemistry of 
talc. "The analyses show that the ratio Mg:Si varies from 1 :1 to 4:3 and the water content from 3 to over 
7 per cent. Most reference books on mineralogy gives the formula as H^g^S^)^ According to this, the 
mineral should carry 63.5 per cent SiO-, but published analyses show a range from 56.86 to 62.10. MgO 
should form 31.8 per cent in the 1 :3 :4 type, but actual analyses vary from 27.9 to 32.40. Alumina, ferric and 
ferrous iron, manganese, and lime are reported in various analyses, although the purity of the material 
analyzed may be open to question in some cases." Gillson intimates that pure talcs are rare and that some 
of the desirable properties of commercial talc result from impurities. 2 

The National Bureau of Standards made tests on a Manchurian talc which had the following properties : 



32.32 per cent 



61.34 per cent 




R 2 3 


0.71 per cent (mostly A1 2 3 ) 




Ratio MgO:Si0 2 :H,0 = 4:5:1.54 

Heat treatment showed that water in excess of one molecule was driven off at 380°C-500°C. No change in 
crystal structure was noted up to 800°C. At 800°C-840°C the talc decomposed into enstatite, amorphous 
silica, and water vapor, abruptly changing the thermal response curve. Only slight changes in the curve 
were noted when enstatite converted to clinoenstatite at 1200 °C and amorphous silica converted to cristo- 
balite at 1300°C. 3 

Nearly every commercial grade of talc can be produced in quantity from the Murphy area, the grades 
depending on the presence or absence of clay, quartz, tremolite, carbonate, rutile and zircon, iron, and sun- 
dry coloring materials. Consequently, chemical analyses may vary over any desired range. Colors range 
from dark gray-green, through a pleasing yellow which was marketed as "Goldex," to a pure white which 
has been measured by the photometer as 100 percent of the whiteness of standard magnesium carbonate. 

In its Report of Investigations 3804 (1945), the Bureau of Mines did not publish complete analyses of 
Murphy talc, but samples from drill cores and shallow pits showed from 1.36 to 2.20 per cent Fe^Oy, 0.04 to 
0.09 per cent CaO, and from a trace to 2.0 per cent rutile and zircon. The following table shows the com- 
plete analyses that are available, together with selected representative analyses from other areas. 

1 C. E. Hunter, Personal Communication, 1047. 

2 J. L. Gillson, 1937. 

3 Nat. Bur. Stds. Jour. Research, RP. 848, 1935. 

Talc Deposits of the Murphy Marble Belt 


Chemical Analyses of Talc 



Fc 2 0* 










































































Maltby.N. C 

Maltby, N.C 

Regal, N.C.... 

Hewitt, N. C. 

Hewitt, N.C 

Murphy, N. C 

Kinsey, N. C 

Murray Co., Georgia. 
Murray Co., Georgia 
Murray Co., Georgia. 

Talladega, Alabama. 

Waterville, Vt 

Gouverneur, N. Y... 

Inyo Co., California. 






TVA files. 

A. S. Furcron and Kefton H. Teague, Talc Deposits of Murray County Georgia; Ga. Geol. Sur. Bull. 53, 1947. 

J. H.Pratt, op. cit. 

Lynn McMurray and Edgar Bowles, Talc Deposits of Talladega County, Alabama; Ala. Geol. Sur. Circ. 16, 1941. 

Average of three samples. 

R. B. Ladoo, Talc and Soapstone: U. S. Bur. Mines Bull. 213, 1923. 

U. S. Bur. Mines, HI 3804, 1945. 

Sierra Talc. Average of five standard samples. 



For background information concerning the genesis of talc in other localities, the reader is referred to 
the excellent summaries and conclusions of Gillson, who made a thorough study of the literature on talc, 
supplemented by personal experience. 1 In his report on the Vermont talc he states : "Few students of talc 
deposits have given the attention to the mineralogy and paragenesis which seem to be necessary to an ade- 
quate conception of talc formation. From the evidence of the Vermont deposits, and the published descrip- 
tions which have been reviewed, the following general conclusions have been drawn : 





Talc deposits are commonly lens-shaped, and of irregular occurrence and extent. 

Talc deposits are replacement deposits in limestone, schists, gneisses, and altered basic intrusions. 

The country rock of talc deposits is almost invariably old, at one time deeply buried probably at the 

time of the talc formation. 

The types of solutions that form talc, whatever was the original rock replaced, first formed amphi- 

bole or a chlorite. ******** These solutions were hot, alkaline, and were at first siliceous 

and carried iron and calcium and some aluminum in addition to magnesium. Later solutions became 

less siliceous and rich in magnesium. 

In many cases, if not in all, these hot solutions were emanations from granitic or dioritic rocks or 

from the acid differentiates of basic intrusions. 

The conditions of depth, high temperature and character of solutions had to be fulfilled in order that 
talc might form." 2 

Harker 3 believed that talc is formed by dynamic metamorphism and Keith 4 was of the same general 
opinion. H. Ries s attributed talc to the action of magmatic solutions. J. H. Pratt* 5 thought the Murphy talc 

1 J. L. Gillson, 1937. 

2 J. L. Gillson, Origin of the Vermont Talc Deposits, Econ. Geol., vol. 22, 1927. 
s A. Harker, Metamorphism, 1932. 

4 Arthur Keith, 1907. 

5 H. Ries, Economic Geology, 1930. 

6 J. H. Pratt, 1900 


Talc Deposits of the Murphy Marble Belt 

resulted from alteration of tremolite. Stuckey concluded that the Murphy talc and associated minerals were 
formed by hot magmatic solutions and listed his criteria as: 

1. Occurrence in irregular lenses. 

2. Gradational character of the contacts between talc and marble. 

3. Silicification of the marble. » 

4. Presence of quartz veins within talc and marble. 

5. Presence of marble "kidneys" within talc bodies. 

6. Presence of non-oriented tremolite in talc and marble. 

7. Microscopic evidence of replacement. 

Stuckey lists the probable sequence of events as: 

1. Formation of Cambrian sediments. 

2. Metamorphism (Appalachian Revolution). 

3. Formation of igneous masses. 

4. Silicification of the marble. 

5. Development of accessory minerals by replacement of marble and quartz. 

6. Development of talc by replacement of tremolite and marble, and coincident development of pyrite 
and magnetite. 1 


A more or less definite zoning within the Murphy marble has been revealed. Listed in descending strati- 
graphic order from top to base, a typical section of the marble, with accumulative depths is as follows : 

Mica schist (ms) 

feet Transition zone 


20 ' 

Actinolitic zone 

105 ' 

Slaty zone 

130 ' 

Mixed zone 




155 ' 

White (talc-bearing) zone 

200 ' 

Mottled zone 

215 ' 

Gray zone 


235 ' 

Blue zone 

275 ' 

Coarse gray zone 


305 ' 

Coarse white zone 

330 ' 

Transition zone 

355 ' 

Ottrelite schist (os) 

The white talc-bearing zone is a dense, fine-grained dolomitic marble which is slightly sandy in places. Some 
of the zones are rather pure calcium carbonate, while others are micaceous and have a high alumina content. 

Evidence of deep-seated magma is found near the talc in the form of diorite sills which lie 300 to 450 
feet stratigraphically above and below the Murphy marble, of pegmatite material which occurs in a mig- 
matitic manner in nearly mica schist, and of gold-galena-bearing quartz veins which are found within the 

In order to prevent excessive repetition, reference is made to data presented in the section on min- 
eralogy of the talc. In summary, the paragenesis in descending order from the youngest to the oldest min- 
erals seems to be as follows : 

J. L. Stuckey, 1937. 

Talc Deposits of the Murphy Marble Belt 29 




Zoisite Muscovite Quartz 

Scapolite Tourmaline Amphibole 

Phlogopite Pyrite Talc 

Amphibole Magnetite Muscovite 

Chlorite Rutile-Zircon Phlogopite 





Some of the late quartz and carbonate have cold solution relationships. 

The talc occurs in ellipsoidal bodies which lie parallel to, and plunge with, local fold axes, and which 
are coincident with definite systems of lineation. 

Although surrounding rocks are severely folded and fractured, excessive movement does not show in 
the internal structures of the talc. Studies of general geology in the area indicate that the talc was formed 
under many thousands of feet of sediments. 


On the basis of foregoing criteria, the following deductions are made : It is obvious that the Murphy talc 
did not result from cold water alteration of original material. Neither does it seem that sufficient magnesia 
and silica were present in the original marble to allow the formation of talc by simple dynamic metamor- 
phism. It is believed that the central, slightly sandy, dolomitic zone allowed the formation of zones of weak- 
ness by dynamic metamorphism. Later hot aqueous solutions of granitic and /or dioritic origin ascended 
along and into zones of structural weakness and at least partly silicified the dolomite. A coincident or later 
wave of hot solutions ascended and formed lenticular talc bodies because an optimum amount of silica, mag- 
nesia, and catalysts were already available. Minute quantities of talc were formed in adjacent marble, but 
either insufficient magnesia, silica, or catalysts were present, or too much alumina and other materials were 
available to allow the formation of more abundant talc. Similar mineralizing solutions are believed to have 
formed the abundant sericite, ottrelite, and other minerals, as well as "pseudodiorite," in several thousands 
of feet of adjacent quartzites, schists, and gneisses. 

These conclusions are in accord with the work of Stuckey and of Gillson except that an intermediate 
chlorite or amphibole phase is not postulated. 


The characteristics of pure and impure talc are utilized in a great number of commercial products and 
processes. Block talc is sawed into crayons for use in marking metal, cloth, and similar materials. Powder- 
ed or granulated talc is used in cosmetic preparations, including soap and lotions ; as a filler and lubricant in 
cloth ; as a filler in paper, rubber, asbestos, and composition materials ; as a lubricant and absorbent in dies 
and molds ; as a pigment and extender in paint ; as a constituent of dispersing agents and pharmaceutical 
supplies ; as a polishing agent ; and as a welding rod coating. More recent and very important uses for talc 
result from its ceramic properties. Certain block (lava) talcs are machined and fired to form parts which 
must stand excessive electric and thermal shock. Powdered talc is used in a talc-clay grog (steatite) extrud- 
ed into molds and fired for purposes similar to the lava talc. Steatite is also used in the manufacture of sag- 
ger bodies, cordurite, and to a lesser extent in the manufacture of whiteware. 

No crude talc is shipped from the Murphy area. Much of the talc is sawed into crayons, packed one 
gross to a carton, and shipped in crates of 24 cartons. All other talc is pulverized at from 90 per cent minus 
100 mesh to 98 per cent minus 200 mesh and shipped in 50 pound paper bags. The pulverized talc is used prin- 
cipally in cosmetic, textile, and food polishing industries. Small shipments sometimes are made to supply 

30 Talc Deposits of the Murphy Marble Belt 

high grade talc in blocks for art work. The Murphy area does not supply the lower grades of talc for use 
as roofing granules or for the other economy markets. However, it is probable that stained, impure surface 
talc could be supplied. 

When the Hewitt mines were in production prior to 1925, ceramic grade talc was utilized for the manu- 
facture of gas tips but no other attempts have been made to enter the ceramic markets. Recent studies by the 
U. S. Bureau of Mines indicate that talc from the Murphy marble can be beneficiated to a degree suitable for 
steatite talc, 1 and it is hoped that producers and research agencies will continue this work. It should be 
emphasized that larger quantities of new grades of talc have become available since the last samples were 
tested, and it is possible that unbeneficiated talc of suitable steatite quality is now available. By adopting 
methods formerly used at the Hewitt mines, the Hitchcock Corporation had firing tests made on talc which 
was mined and allowed to cure in the cool darkness of the Nancy Jordan Mine for about two weeks. The re- 
sulting fired shrinkage and checking was notably less than that of freshly mined talc. 

Mining and milling costs in recent operations are not available, but it is believed that normal estimating 
methods can be applied with a fair degree of accuracy. Accurate prices of processed talc can be obtained only 
through reputable buyers, but it is probable that the average price of talc products from the Murphy area 
exceeds $50 per ton, f.o.b. Murphy area, including both crayons and pulverized talc. Prices of pulverized talc 
are quite variable but talc crayons are fairly well stabilized at the equivalent of from $350 to $400 per ton in 
in individual cartons. 

Talc reserves in the Murphy marble belt are more than adequate for long term operations. Indicated re- 
serves on three properties alone amount to a quarter of a million tons crude, and probable reserves are pro- 
portionally high. There is still plenty of room for additional exploration work with good chance of success 
as compared with other types of mineral exploration, and much of the "guess work" has now been removed. 

The writer has been told by reputable talc producers and buyers that the Murphy talc can and does com- 
pete favorably with standard and premium talc of California, France, and Italy. One of the principal barriers 
to rapid expansion has been the past history of sporadic, undependable talc production in North Carolina, 
but the industry is now firmly entrenched and is building a good reputation among buyers. One other re- 
straining factor has been the exotic sales appeal of imported foreign talcs whose qualities easily may be 
equaled in this country. The needs today are increased exploration by core drilling, exploitation of deposits 
already known, utilization of low grade material, continuance of scientific mining and milling methods, close 
laboratory control, and more diligent sales promotion. These, together with the freight cost advantage over 
more distant deposits, can easily raise North Carolina to higher rank as a producer of superior grades of talc. 


The locations described are shown by corresponding numbers on the accompanying geologic map. These 
are locations of talc outcrops, prospects, old and new mines, and sites of exploration of one kind or another. 
Descriptions of the older work has been obtained from published material and from information supplied by 
persons who were associated with the work. Sources of information not received from published literature 
will not be acknowledged in every instance. 


In 1939 the Carolina Talc Company did core drilling work on the west bank of Rapier Mill Creek, 100 
feet north of Georgia Highway 60 and about 500 feet north of the Georgia-North Carolina line. It is re- 
ported that six holes were drilled, encountering white and light gray marble and only a few small specks of talc. 
There are no outcrops in the vicinity to indicate the presence of talc. The property was core drilled because 
of the presence of a red soil that was considered indicative of talc. No core records were preserved. 


It is reported that several small shipments of talc were made from this property. The appearance at 
present is of a number of open pits, made apparently at random on the Cearly property in the bend of a clay 
road leading northwest from Culberson. Other than rare small talc scales and a light gray plastic clay, there 
is no evidence either of talc or marble. 

U. S. Bur. Mines, R.I. 3804, 1945. 

< Q 


H Z'W 


ft .m 


W >H 

25 Wfc, 


£ W .-! 


< ZO 


2 < 



^ j 




32 Talc Deposits of the Murphy Marble Belt 


In a railroad cut, one mile northeast of Culberson and 500 feet southwest of an L&N railroad trestle over 
Rapier Mill Creek, talc lenses and stringers up to 18 inches across crop out in a clay bank. Occasional ledges 
of marble are exposed in the cut and there is a small abandoned marble quarry 1,000 feet to the southwest. It 
is reported that the marble quarry did not reveal talc signs of any kind and that the marble was dark gray s 
white, and multicolored. On the basis of talc exposures in the railroad cut, three core holes were drilled be- 
tween the talc outcrops and the marble quarry but no success was achieved and core records were not pre- 


In the fall of 1945 and spring of 1946 the Mauney Mining Company did a little over 2,600 linear feet of 
core drilling for talc on the land of P. A. Mauney, about 1,500 feet southwest of Kinsey. The first 12 holes were 
located from the appearance of talc fragments in the overburden in a nearby railroad cut. A ledge of tremo- 
litic marble in the railroad cut also showed small scales of talc. These first holes, accounting for 1,875 linear 
feet, intercepted nearly all of the upper stratigraphic half of the overturned marble formation without show- 
ing more than an inch of talc. These first holes, however, were of especial value when correlated with infor- 
mation from other sources, and they represented a key to the subdivision of the marble formation. As a result 
of the newly acquired data, four additional holes were drilled and the talc-bearing horizon was intercepted, 
although no talc was found. More than 1,000 feet of strike length remains to be explored on this property to 
the northeast toward the old Kinsey Mine, and there is no reason to assume that additional work would be 
illogical if close geologic control is maintained and if the data from previous drilling are utilized. 


Near the southwest bank of the Nottely River, downstream from Hall's Ford and 300 feet northeast of 
Kinsey, an abandoned marble quarry now occupies the approximate site of the old Kinsey Talc Mine. A num- 
ber of old caved shafts or pits can be seen for 100 feet southeast of the quarry. The quarry seems to include 
a small part of the white marble zone, full sections of the mixed zone and slaty zone, and a part of the actino- 
litic zone. One four-foot ledge of silicified marble can be seen on the caved southeast wall of the quarry and 
five lenses of talc, from three inches to twelve inches thick, crop out in the same place. Quantities of soft 
talc appear on the surface and in clay overburden, but these may come from the spoil of the older workings. 
Three core holes were drilled by the Cherokee Minerals Company in 1938 but core recovery was poor and no 
signs of talc were revealed. Two of the holes were located southeast of the L&N Railroad, and the third hole 
was on the northwest side nearer the quarry. It is believed that these core holes were not indicative and that 
additional prospecting would not be out of order. 

When J. H. Pratt visited the Kinsey Mine around 1900, he reported that the talc lay in flat lenses wholly 
within the marble and associated with siliceous material. There were two tunnels, one 75 feet long, at levels 
10 feet apart. Pratt reported that some of the talc blocks weighed a thousand pounds and that the mill pro- 
duced six tons of "flower" talc per day. The workings probably extended under the L&N railroad. 


The Carolina Talc Mine is also known locally as the Bailey Mine, Notla Mine, and Kinsey Mine (not to 
be confused with Location No. 5). It is situated on the right floodplain of the Nottely River 3,000 feet north- 
east of Kinsey and 1,900 feet west of Rogers Chapel. The first reported prospecting was done by H. S. Pred- 
more and/or the Binney and Smith Company around 1907-08, and the first shaft was sunk in 1916. From 
1926 until 1934 the property was operated through the Notla Talc Company by Binney and Smith. The Caro- 
lina Talc Company took over the property in 1934 and carried on successful operations until July 23, 1938, 
when high water from the Nottely River spread out over the flood plain, caving the mine from the surface 
and flooding it. Hiwassee Dam was nearing completion at the time and no attempt was made to resume op- 
erations since the surface level at the mine soon would be under six feet of water. It was estimated at the time 
that about 25,000 tons of talc remained underground, but more recent studies indicate that more complete 
core drill information probably would have resulted in higher estimates. 

Talc Deposits of the Murphy Marble Belt 

Fig. 7. — Model Showing Underground Workings at the Carolina Talc 
Mine. White Parts of Pegs Represent Talc Encountered in 
Drill Holes. Looking Northwest. 

Entry to the mine was by way of an eight by ten foot shaft, vertical for 116 feet, and then following the 
steep footwall to a total depth of 155 feet. Drift levels were opened from the shaft at the 56 foot, 82 foot, 
104 foot, and 116 foot levels and combination drift-slope mining was carried on in both directions along the 
axis of the talc body. Talc was brought down from the roof and face by barring or by shooting with 40 per 
cent and 60 per cent dynamite, or a combination of both methods. Underground water flow from the nearby 
Notteley River caused potential hazards, and two bulkheads were required to hold back a nearly unrestricted 
flow through open cavities. Average water inflow during normal operations amounted to about 250 gpm, 
but maintenance facilities included three pumps rated at 2,500 gpm each for use during the rainy season. 
Two pumps of 3,585 gpm total capacity were held in reserve. 

Crude talc was hoisted from the mine by an electric three-drum hoist having 14 by 24 inch drums. The 
talc was pulverized in a Bethlehem 4-roll crusher incorporated with an air separator having a capacity of 
1,500 pounds per hour at 98 percent minus 200 mesh. Crayons were sawed with one block saw, one slab saw, 
and five finishing saws. Average labor for the mine and mill consisted of around 20 men. Drill cores at the 
Carolina Mine were logged only to differentiate talc and marble; the core records do not reveal the detailed 
mineralogy or structure which characterized the cores. 

The talc deposit apparently was similar in size and general configuration to that at the Nancy Jordan 
Mine (Location No. 10), but there seems to have been a greater amount of mixed talc and marble and a less 
definite outline of a main talc body. The enclosing marble had a strike and dip of about N40°E, 55°SE; the 
talc plunged approximately 15° in a direction S25°W and dipped with the marble. Hangingwall and footwall 
structures were more evident than at other localities, and it is near the footwall particularly that a slate rock 
may have been partially serpentinized, according to older descriptions of underground conditions. Older 
reports indicate the probability that distinct lineations of cleavage intersections were important structures, 
with trends coincident with the plunge of the talc. In a manner similar to the Mulberry Gap deposit (Loca- 
tion No. 7), it is possible that the northeast end of the Carolina deposit has slumped vertically downward as 
a result of mass disintegration of the underlying marble. Associations of silicified marble around the talc, 
and as kidneys in the talc, were similar to associations in other talc bodies in the area, as was the presence of 
"mineralized" (pyrite, phlogopite, scapolite, actinolite,etc.) marble in those places where the talc normally 
might have been but specifically was absent. 

The Carolina Mine supplied some of the finest quality talc ever produced in North Carolina. Standard 
grades of pulverized talc were supplied in large quantity and approximately 4 per cent of the talc was cut into 


Talc Deposits of the Murphy Marble Belt 

crayons. Mr. J. W. Bailey, President, of the Carolina Talc Company, has graciously given the writer per- 
mission to publish the production and cost data in Table II. Production figures for the years prior to 1930 
are not available. The Carolina Talc Company was solely an operating company for Notla Talc Company and 
thereby showed neither profit nor loss. 

table II 
Production and Cost Data — Carolina Tai.c Company 


•Crude Talc 




3 Grinding 

'Crayon Cost 







$ 10.45 

t 11.26 

t 118.59 




62 .47 6 


151 .70 



1935 - 

257 .55 



1937 - 


Total --- 




$ 81 .28 

$ 60.04 

$ 1,261.73 




$ 10.11 

$ 7.50 

$ 157.71 

1 Short tons. 

2 Per ton crude. 

3 Per ton powder. 
* Per ton crayons. 

6 Very low and very high cost figures reflect differences in the degree of expansion in any single year. Variations tend to balance over 

long periods. 
Note: Certain sales costs and incidental expenses are distributed thorughout these costs 


The Mulberry Gap talc mine is situated on marginal land of Hiwassee Lake and is licensed by the Ten- 
nessee Valley Authority to the Minerals and Metals Corporation, Murphy, North Carolina, of which H. G. 
Robinson is President, F. C. Bourne is General Manager, and J. W. Bailey, Jr., is Superintendent. The mine 
is located 2,500 feet northeast of the Carolina Mine and 1,400 feet northwest of Rogers Chapel, on the right 
bank of Nottely River. Older workings at the same locality have been called, at various times, the Hillyer 
Mine, the Munsford Mine, the Davis Mine, and the Old Mill Mine. 

In 1900 J. H. Pratt described the mine as owned by the Atlanta Talc, Mining and Manufacturing Com- 
pany, of which Judge George Hillyer, of Atlanta, Georgia, was President. There were three shafts, 100 feet 
apart along the line of strike, each shaft being 60 feet deep and penetrating the talc for 27 feet. "The 
footwall of quartzite is but 16 feet from the shafts and is dipping nearly 30° to the southeast. The width of 
the (talc) bed is known to be 40 feet .... A little to the northwest of the line of shafts and 300 feet to the 
southeast (southwest ?), a tunnel 100 feet long was run along the quartzite (silicified marble ?) contact 
and good talc encountered. 

"This mine has yielded several thousand tons of the finest quality of talc, but practically none of it was 
compact enough to be used in cutting into pencils." 1 

It is reported that several later attempts were made to reopen the workings but water flow prevented 
success. H. S. Predmore began investigations sometime after 1940 and the property was taken over by the 
Minerals and Metals Corporation. Production began in 1944, but this new work did not involve the older 
openings which lay to the northeast and southeast. 

Entry was made through an inclined shaft, down a vertical winze, then along a cross-cut and a drift 
within good white talc was opened to the northeast. In the meantime, a small stope was made near the 
vertical winze. Poor underground conditions halted work in the northeast-running drift and Shaft No. 2 
was begun. Because of slow progress and a desire foe more immediate production, Shaft No. 3 was begun 
and, by good fortune, it intercepted 26 feet of talc. Shaft No. 2 was continued and all three shafts were 

1 J. H. Pratt, 1900, p. 20 

























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Talc Deposits of the Murphy Marble Belt 37 

subsequently connected by drifts and crosscuts. A small crosscut was made to the northwest near Shaft No. 2 
. and intercepted a steep, six-foot body of talc that was too badly clay-stained for use at that time. All this 
work was done under the managership of W. O. Hoffman and later under George S. Stauning. 

Underground conditions became uncertain and a study of the structure indicated the possibility that 
the southwest-plunging talc body would be accessible from an open pit to the northeast. A series of 12 core 
holes were drilled and plans were formulated to make a pit 110 feet long by about 55 feet wide, involving 
some 23,000 cubic yards of earth excavation. Excavation has now been completed and successful open cut 
mining is underway. An estimated 15,000 tons of talc will be available through this phase of the operation. 
Current plans call for a later extension of the open cut work to overlap the older operations, and the newer 
underground openings will be re-entered. 

Approximately 1,700 tons of talc were removed from the underground openings. Crayon talc was sawed 
at the company's own mill in Murphy and the powdered talc was, and is, custom ground by the Hitchcock 
Corporation near Murphy. The talc is of average grade, having a color rating of from 87 to 93 per cent of the 
whiteness of standard magnesium carbonate. The upper portion of the talc in the open pit has badly stained 
areas but better quality is encountered with increased depth. 

The absolute configuration of this talc body is not known, although it is certain that structural and min- 
eralogic tendencies are nearly identical to the other talc deposits of the area. Minimum length and width in 
places are 300 and 100 feet, but the average thickness is about 10 feet, less than either the Carolina or Nancy 
Jordan deposits. All of the exposed wall rock is more or less silicified, as are the rock "kidneys" inside the 
otherwise pure talc, but quartz-free marble lies a short distance away. It is probable that the northeast end 
of the talc body has slumped because of disintegration of the dolomitic marble which supported it. This 
slump gives the initial impression that the talc has a double plunge (Plate 3). 


This property is owned by the Tar Heel Investment Company of Asheville, North Carolina. It is situa- 
ted near Sneed Branch, two miles southwest of Murphy and 4,500 feet northeast of the mouth of Cane Creek. 
A number of pits have been dug along an old logging road, and white talc shows at the surface in several 
places. It is reported that two or three tons of talc have been removed from the pits. Although no definite 
evidence is present, it is possible that the talc has been transported by creep and that a normal outcrop posi- 
tion would be several feet to the southeast. 


About 2,600 feet along the marble and to the northeast of Location No. 8, and situated on the same Tar 
Heel property, talc was revealed in the bank of a trail while road repairs were being made. The owners drill- 
ed about six core holes down dip from the talc exposure, intercepting talc in only one of the holes. It is 
possible that this talc had been transported a short distance and was on the up-dip (northwest) side of the out- 
crop position. The owners are planning to do additional core drilling all along the strike from Location No. 8 
to Location No. 10. 


The Nancy Jordan talc mine, owned by the Tar Heel Investment Company and operated by the Hitch- 
cock Corporation, is 4,500 feet southwest of the Hiwassee River at Murphy and 1.9 miles northeast of the 
mouth of Cane Creek. The property has been owned by the Hitchcock heirs for a great many years, being 
part of a tract which extends from the Hiwassee River to the Nottely River. 

Nancy Jordan Mine was first discovered by the Tar Heel Investment Company around 1941 when a core 
drill program began at Location No. 11 and extended across Nancy Jordan Gap to about Location No. 9. The 
site was by-passed by the first line of holes because they were located too far to the northeast. When the en- 
tire program appeared to be doomed to failure, the drill was brought back to the approximate location of 
the present mill building and a hole was put down on the strength of an outcrop of sandy marble in the road 
bed. This hole too was barren, but one last hole was located 100 feet farther to the southeast and twenty- 
three and a half feet of talc was cored. 


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40 Talc Deposits of the Murphy Marble Belt 

The mine shaft is a two compartment, 10 by 12 foot collared shaft, with ring timbers and two inch lag- 
ging- extending to the 80 foot level where the timbers are securely anchored. From 80 feet to the 208 foot 
bottom the shaft is in solid marble and requires no support. Working levels are at 168 feet (Elev. 1513) and 
196 feet (Elev. 1485) where crosscuts enter the talc body about 20 and 10 feet, respectively, from the shaft. 
A stope on the 1513 level gives access to the 1530 level, at the northeast end of which is a second stope. The 
1530 stope is connected to the northeast end of the 1485 drift by a small, steep ladder-chute raise. A drift 
extends southwestward from the main crosscut on the 1513 level and from this drift a small crosscut connects 
the main talc body with several large pockets of very white talc to the southeast. Approximately 40 tons of 
talc has been mined from these pockets to date. From the 1485 foot level an incline extends southwestward 
down the plunge of the talc body with the incline floor generally following the footwall along the principal 
axis of the body. After reaching an elevation of about 1440 the incline gives way to a level drift. 

All stopes and some of the drifts are square-set in an excellent manner, with 5 ] /o by 5^2 by 7^2 foot sets 
using 7 by 9 inch pre-cut oak timbers, and thus far there has been no trouble from caving. Water flows come 
almost entirely from surface drill holes. A 170 gpm pump operates about one hour per day to keep all sumps 
at safe levels. All underground lighting is by electricity with conduit entries down the shaft. Operating 
signals between shaft head and mine are made by blinking the electric lights. Skip signals are made by a 
hand-pulled bell cord. 

A sullivan air operated post core drill is used for underground exploration, and blast holes are made with 
stoppers and jackhammers. The necessary shooting is done with Special D. explosive. In crayon grade talc, 
as large blocks as possible are dropped on a pad of fine talc to prevent splitting and the blocks are sawed to 
handling size with an ordinary two-man cross-cut saw. In talc of pulverizing grade, shooting is heavier to 
produce as good fragmentation as possible. Talc is shoveled or placed by hand into 1200 pound buckets, 
which in turn are trammed to the shaft on hoist-operated flat cars. Buckets are hoisted up the shaft by 
means of a steam hoist converted to air, and the talc is dumped into a tilt-dump car and trammed to stor- 
age bins. 

Crayon talc is chuted to the crayon mill where it passes through a saw line as follows: A block saw 
cuts to handling size and establishes the length of the crayons; a slab saw cuts to the proper width; finish 
saws end the operation by giving the correct thickness ; when necessary, a dowel cutter makes one-fourth inch 
round pencils from one-fourth by one-fourth inch square crayons five inches long. Finished crayons go suc- 
cessively to graders, packers, and craters and are ready for shipment. 

Pulverizing talc goes from the storage bin to a primary hammer mill by conveyer belt, then by belt to 
a 10-ton feed bin. The talc is then delivered to a Raymond roll mill which is integrated with a double whiz- 
zer air separator, all in closed circuit and feed controlled by pneumatic pressure. The finished powder is 
placed in 50 pound paper bags by a two-tube Bates Bagger and trucked one mile to box cars. The quality of 
the finished product is controlled by taking bag samples at half-hour intervals and testing with a photo-electric 
comparator against standard magnesium carbonate. Grading is by color and whiteness according to the ICI 
tristimulus filter system of the National Bureau of Standards. By blending different qualities, operations 
are based on a standard product having a whiteness rating of 90 per cent of magnesium carbonate. Fineness 
of grind is checked with a Hageman gauge. Talc from the Nancy Jordan Mine does not go to any of the econ- 
omy markets, but is used principally for crayons, cosmetics, textile bleacheries, rice polishing material (grit 
free) and similar grades. It is believed that this talc has excellent opportunities for uses of pulverized talc 
in ceramic industries. 

F. C. Bourne is Treasurer of the Hitchcock Corporation and General Manager of the Nancy Jordan Mine. 
J. W. Bailey, Jr., is General Superintendent. Other personnel are a technician-secretary, diamond driller 
and helper, six mine workers and sixteen mill employees, in addition to several men who do general work 
around the plant. The company sponsors an employee health and accident insurance program and carries out 
a bonus system based on safety, attendance, production, and length of service. 

More is known of the Nancy Jordan talc body than of any other talc in the entire area. In addition to the 
underground work, there are 23 fairly well-spaced core holes of which 14 are recorded in great detail. Studies 
included examination of core records, survey of mine openings, and preparation of surface contours, top of 
rock contours, top of talc contours, talc thickness contours, and geologic sections, and limited petrographic 
work. Partial chemical analyses were also available. 


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42 Talc Deposits op the Murphy Marble Belt 

In plan-projection, the talc body is shaped somewhat like the hull of a sail boat; the keel is down dip and 
slightly down-plunge from the center. Again in plan, maximum length and width are 690 feet and 144 feet, 
and maximum vertical thickness is about 50 feet. More accurate dimensions are shown in the accompanying 
drawings. (Plates 4 and 5). The southwest end of the talc body was delimited by projection and represents 
a probable minimum. On this basis and discounting all extraneous talc stringers and pockets and all zones 
of mixed talc and marble, it is calculated that the body contains slightly under 100,0,00 short tons of talc. 

The average strike and dip of the marble underground is N40i/2°E, 52°SE; this is the approximate av- 
erage strike and dip of the talc layers as well. Average plunge of the talc body is about 18° in a direction 
S22°W, but the overall plunge is 14° in a direction S25°W. Configuration of the body in detail is somewhat ir- 
regular, since the plunge is variable and the footwall and hangingwall are subject to rolling around the long 
axis of the body. The principal internal structures are similar to those presented in the general discussion 
of talc bodies. Two distinct cleavages intersect to form a lineation coincident with the plunge of the talc 
body, contributing in part to the fibrous nature of the talc. Variations in grade, from dark "sheened" talc to 
good white talc, are controlled by both dip and plunge, and talc grades are repeated both across and along dip, 
strike, and plunge. These changes make feasible good control in selective mining of the various qualities as 
desired. Joints and faults have little economic or geologic significance. 

Beginning half-way down the plunge of the talc body, silicified marble is an important constituent of the 
wall rock and of the small marble "kidneys" which are sometimes contained within the talc. It is in this 
siliceous material that most of the tourmaline in the mine can be seen. Phlogopite, pyrite, and smaller 
amounts of quartz are contained in wall rock of the northeastern half of the body. Tremolite crystals of mega- 
scopic sizes are not often found in or immediately near the talc, but minute tremolite fragments show in some 
of the talc when observed under the microscope. 

Mining methods are aimed at maximum crayon production. Openings are kept as low (down dip) with- 
in the body as possible in order that overhead stopes may be utilized to best advantage. In this way it is ex- 
pected that nearly 100 per cent extraction will be realized when the body is ultimately exhausted. Drifts and 
crosscuts have been maintained at a size suitable for one standard set of timbers. The openings have been 
designed to give maximum development information while allowing sufficient talc production. 

Mr. F. C. Bourne has kindly consented to the publication of the following production data which represent 
total production to June 30, 1947 : 

table hi 

Talc Production — Nancy Jordan Mine 

Year Crayons Produced Powder Produced 

1945a ' 200.65 sh.tons 2080.43 sh.tons 

1946b 152.78 1875.47 

1947c 69.55 1976.11 


29 Months 422.98 5932.01 

Total Production (29 months) _ _ - 6354.99 sh.tons 

a. February-December 

l)- January-December 

c. January-June 

Based upon production figures for 1946, as published by the U. S. Bureau of Mines, x it is estimated that 
the present average crayon production of the Hitchcock Corporation is equal to about one-fourth of the total 
United States production. 

U. S. Bur. Mines, Mineral Market Report, MMS. no. 1544, 1947. 

Talc Deposits of the Murphy Marble Belt 




Crude ore bin for 
pulverizing talc 
200 ton capacity 

H Chute 

Crayon talc 



Specialty Products 



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closed circuit 


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Figure 9 

44 Talc Deposits of the Murphy Marble Belt 


The Cold Springs Mine was formerly owned by the Tar Heel Investment Company but is now owned by 
the TVA as a part of Hiwassee Reservoir land. Two shafts, approximately 65 feet deep, are located one on 
either side of a gravel road at the junction of the Murphy Town Park road. Several different people, the last 
of whom was F. C. Bourne, have attempted Lo operate the mine at various times, but poor ground conditions 
and excessive water, together with insufficient exploratory work, have contributed 'to unsatisfactory results. 
It is reported that a total of about 1,000 tons of talc has been taken from the two shafts. Information about 
the geology underground is too conflicting to report here. 


Small quantities of talc crop out in the bed of Valley River, 400 feet from its mouth. Stringers up to 
three inches thick are contained in dense, white, finely tremolitic marble, but stream debris and deep water 
prevent further observations. Mr. Harry Quintrell, of near Jasper, Georgia, attempted to sink a shaft in 
the peninsula between Hiwassee River and Valley River, and fairly large quantities of talc were supposedly 
intercepted before excessive water flow halted the work. It is believed that the Quintrell shaft was 30 to 35 
feet deep and that production was never achieved. 


This prospect is known as "Section 6," being on a tract of land of the same name. Yellow surface talc 
has been recognized here for a great many years although no prospecting has been done other than the dig- 
ging of a few small pits and trenches. Stained talc appears at the surface over an area of 1,000 square feet, 
and siliceous, tremolitic boulders may be seen in the fields and in a nearby creek. In 1946 the Hitchcock Cor- 
poration obtained a lease on the property for the purpose of diamond drilling for the talc body which sup- 
posedly furnished surface indications. A total of six core holes was drilled, although two of the holes were 
abandoned shortly after intercepting top of rock. The four completed holes satisfactorily intercepted the 
normal talc-bearing zone where the rock was confined to white barren marble and to silicified marble and 
zones of considerable tremolite. One of the holes disclosed thin veinlets of galena in the fractures of an 
otherwise pure dolomite. Correlations indicate that the original talc body has been almost completely eroded 
and that only transported talc can be seen. This does not mean that other talc deposits could not be present 
a short distance away. 


This location is noted because of data which indicates the probable position of the white marble zone in a 
concealed area. A churn drill, in drilling for water, intercepted dark, blue, coarse-grained, heavily graph- 
itic marble at a depth of 105 feet, and continued in the same type of rock for about 40 additional feet. By 
applying the principle listed in the section on prospecting for talc, the position of the white marble zone can 
be calculated. No indicative surface outcrops of any kind are perceptible in the vicinity. 


Forty-six hundred feet southwest of Regal Station, on property now owned in part by J. B. Moore, and 
in part by the Southern Railway System, a ledge of silicified marble outcrops in a railroad cut and is sur- 
rounded by a clay residuum which contains irregular patches of white and yellow talc. Just on the top edge 
of the cut, nearly opposite Mr. Moore's house, are the remains of an old shaft which was sunk sometime 
around 1900 by a Mr. Heighway. It is reported that a good grade of block talc was removed and sold, and 
that the operations were stopped because of interference with railroad operations, but no other information 
is known. 


Overlapping Location No. 15, a block of land has been leased by J. P. Jennings, Jr., Agent, of Asheville. 
On the basis of the data listed under Location No. 15 above and of a general knowledge of the position of the 
Murphy marble, the lessee conceived a plan to make a geophysical survey over a test area and check results 

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46 Talc Deposits of the Murphy Marble Belt 

by diamond drilling. A total of 12 ranges, on 100 foot centers, was surveyed on nominal 25-foot centers, 
using a Hotchkiss Super Dip magnetometer. The geologist did not submit any detailed locations of the geol- 
ogy, except those which were needed to provide sufficient coverage, but a detailed geologic plan and section 
was prepared in advance and held for final correlation. Corrected profiles of the Hotchkiss readings showed 
distinct anomalies near the inferred marble-schist contacts at top of rock, as well as near the inferred position 
of the silicified white marble zone. Variations amounted to from 80 to 270 Hotchkiss units at 2° sensitivity 
setting, with a base norm of 125 Hotchkiss units. The diamond drill check holes have not been put down at 
this time. It should not be assumed, from this discussion, that the Hotchkiss survey is either affirmed or de- 
nied, nor is it inferred that talc is or is not present in the area described. However, the data presented un- 
der Location No. 15 are indicative of good possibilities for talc. 

LOCATIONS NO. 17 & 18 

The Regal Talc mines are situated about 2,500 feet northeast of Regal Station and 4,700 feet southwest 
of Tomotla School. Lovat Frazer is in charge of the property. Probably as many as 25 pits, shafts, and adits 
have been opened within several hundred feet of the present main shaft, although significant production has 
not been realized so far as is known. The main shaft is reported to be about 80 feet deep, with short drifts 
branching out at two levels. None of the openings have encountered hard rock but masses of badly stained 
talc were found. From the meager information obtainable, and in view of the known position of the marble 
formation, it is believed that these openings are located too far to the northwest to intercept commercial talc 
in good quantity, and that most, if not all, of the talc intercepted thus far has been transported from a few 
feet to possibly a hundred feet or more. 


Several pits have been dug at a point 500 feet northeast of Location No. 18. It is reported that some talc 
was found but it apparently was not of sufficient importance to warrant further work at the time. There are 
no surface indications present at this time. 


The Hayes Mine is now represented by large depressions on either side of a dirt road on the right bank of 
Valley River at the Tomotla stream gaging station. A dense, white, impure dolomite can be seen in one of the 
depressions and on the river bank nearby, and boulders of talcose quartz lay on the surface until just a few 
years ago when student collectors exhausted the supply. Pratt (op. cit.) described the deposit as an open cut 
about 60 feet long, 40 feet wide and 30 feet deep, following down a talc-marble contact on the southeast side. 
He stated that borings showed considerable width and depth of the talc and that test pits 50 feet to the south- 
west and 200 feet to the northeast indicated a continuation along the strike. About 1,000 tons of talc were re- 
moved prior to 1900, of which only one-fourth was of "first" grade. It is stated, however, that stain and 
grit decreased with depth. 


On the northwest side of the Southern Railway at Maltby, a large open pit has been excavated in search 
of talc and several core holes were drilled nearby. The last work at this location was done by J. W. Bailey in 
1939-1940. Although considerable talc has been discovered near the surface, tremolite was present in such 
copious quantity as to render impracticable any economic development. This is the location of the Southern 
Mineral Company operations described by Pratt in 1900. At that time the mine was 70 feet square by 10-20 
feet deep, with a 15 foot shaft at the center of the pit and two 30 foot shafts at the southwestern end of the 
pit. The southeast talc wall was of marble and the northwest wall was of "quartzite." It is reported that 
1,000 tons of talc were mined prior to 1900 and that a well-equipped mill had a capacity of 15 tons of "flower" 
talc per day. 


This, apparently, is what Pratt called the Valleytown Mineral Company property, situated on the south- 
west side of a dirt road, northwest of the Southern Railway, and 2,800 feet northeast of Maltby. Approxi- 


If "-"^ ^v,V wvw ^ w 













V A 


i — i 




k 2; 





a ~ 








co 2 










2 "S 

*-. o " 

•=z S 

.2 3 

o p 


48 Talc Deposits of the Murphy Marble Belt 

mately 200 linear feet of trenches and pits have been dug to an average depth of eight feet, disclosing heavily 
tremolitic talc similar to that at Maltby. Tremolite crystals as much as 20 inches long have been found here. 


Across the dirt road mentioned above, and 350 feet northeast of Location No." 22, three shafts of un- 
known depth have been sunk for talc. The first, and most successful, work was done by the Biltmore Talc 
Company, of Asheville, North Carolina, at about the time of World War I. It is reported that several drifts 
opened from the shaft at about the 60-80 foot level, probably trending northeast since the talc was supposed to 
have plunged northeastwardly at a low angle. Several hundred tons of "good grade cosmetic talc" is supposed 
to have been taken from the mine. 

Around 1940, W. O. Hoffman sunk a shaft which was superimposed exactly upon the old Biltmore shaft, 
but operations were stopped before any development work was done. In 1946, W. A. Sherril, of Murphy, began 
a shaft to the north of the Biltmore location but this work too was abandoned without finding talc. 


About 600 feet west of Hyatt Creek, in the village of Marble, shafts of unknown dates were sunk on 
either side of U. S. Highway 19. It is not reported that talc was encountered although a mottled marble out- 
crop under the trestle across Hyatt Creek indicates the possibility that talc could be present in the general 


On property of W. B. Hartsfield, of Atlanta, Georgia, about 1,500 feet north of Moss Cemetery and 1,500 
feet southwest of the Columbia Marble Company plant, 13 core holes and a shaft were put down around 1944. 
The drill holes did not intercept talc and no records of the cores were preserved, but the shaft encountered 
boulders of talc, tremolite, and siliceous marble at a depth of about 55 feet. Definite bed rock was not 
found in the shaft. 

Several additional core holes were drilled in 1946 and detailed core logs were made. Core data showed 
that the marble formation was in normal position (not overturned) and subject to broad folding, and that 
any original talc at the specific location had been eroded. Talc encountered in the shaft apparently was trans- 
ported material contained in alluvium and residuum. This does not mean that other talc deposits could not 
be in place in the general vicinity. 


It is reported that talc was found in a 66 foot shaft on the J. F. Palmer property, but reliable informa- 
tion about the general conditions could not be secured. 


J. W. Bailey put down a shaft on property of the Columbia Marble Company and some talc was found, 
but the shaft was located in swampy ground and work was abandoned because of excessive water. Later 
diamond drilling for marble by the Columbia Company indicated that Mr. Baileys' choice of a shaft site was 
logical so far as the marble's lithology was concerned, but no talc was encountered in the drill holes. 


On Junaluska Creek, at Andrews, 3,500 feet southwest of U. S. Highway 19, the Weber Company, of New 
York, put down several shafts near the southeast marble contact. Only a sericitic and possibly talcose, black 
and green slate was found. 

Talc Deposits of the Murphy Marble Belt 49 


Shallow pits and inclines were put down in a marble outcrop on property of the Nantahala Talc and 
Limestone Company, 250 feet northeast of the mouth Jenkins Branch and 2,700 feet west-southwest from 
Topton School. By hand-working small (12-18 inch) pockets, some talc was removed before water flow 
and a lack of adequate equipment brought the work to a halt. Other digging was done in talcose sericite 


About 1,000 feet northeast of Location No. 29, development work was only slightly more extensive and 
successful. Talc pockets contained in a strongly sheared marble produced some low grade talc, mostly quite dark. 
The marble is less than 100 feet thick here, so that any further exploration work would be restricted to a 
small area. 


Just to the northwest of U. S. Highway 19, 400 feet southwest of the Macon County line and one mile 
southwest of Nantahala Station, a small talc body was discovered and r lined by the Nantahala Talc and Lime- 
stone Company. The strike and dip of the marble are N32°E, 70°SE. The talc plunged about 30° to the 
northeast. Silicified marble, with additional quartz in the form of rounded sand grains, is in clear evidence 
on either side of the talc body and for 100 feet or so along the strike as well. The talc body was about 30 
feet long and 6 feet wide and about 4 feet thick in the larger sections, thinning to a few inches up and down 
the dip and along the plunge. It apparently contained many marble inclusions. The talc was of good clear 
color, somewhat sheared, and exhibited curved grain and very hard, glazed surfaces. Additional work has 
not been done since the bulk of the small talc body was removed. 


High over the right bank of Ledbetter Creek, 2,000 feet northeast of Location No. 31, an adit was start- 
ed in talus material by a Mr. Lunsford of Nantahala. Talc fragments were found in the debris, but loose 
ground and inadequate equipment made extensive work impractical. 


On the northwest contact of the Murphy marble, 1,200 feet northwest of Nantahala Station, a great deal 
of digging and tunnelling has been done in a talcose, serpentinized schist, apparently outside of the marble 
formation. Nearly all of the holes are now caved and covered with debris. 


This prospect, also worked by Mr. Lunsford, seems to be within the marble formation, but talus material 
is quite deep. Adjacent outcrops of marble are impure, showing large quantities of chlorite, quartz, and 
micaceous material. Mr. Lunsford is supposed to have sunk a shaft by himself and taken out some talc, but 
the prospect is now abandoned. 


The Nantahala Talc and Limestone Company has done core drilling in a draw behind Hewitt Church. 
The first hole was located over the Nottely quartzite and was abandoned when true conditions were made 
known ; six holes were drilled in the marble formation but incomplete core recovery did not allow a good 
picture of local conditions. It is believed that the talc-bearing zone of the marble was intercepted in at least 
three of the six holes, but only a few odd fragments of talc were recovered. Principal variation from a nor- 
mal sequence of marble zones was in a wide distribution of chlorite and pink marble bands. Otherwise, the 
sequence of blue, gray, mottled, white, and mixed and slaty marble was satisfactory. 

About 100 feet north of the drill holes, and on the nose of a small ridge, an adit goes back into the hill for 
about 70 feet, obliquely crossing the strike. It is reported that several pockets of talc were encountered in 
the opening and some talc may be seen on the old dumps. 


Talc Deposits of the Murphy Marble Belt 


Immediately behind Hewitt School, on a flat area just north of the Southern Railway, considerable talc 
has been extracted from open pits and shallow adits. Recently one core hole was drilled at this location, but 
core recovery was entirely unsatisfactory. The discussion of Location No. 37, below, applies in part to this 
locality. » 

LOCATIONS NO. 37 & 38 

Number 37 indicates the old Hewitt Shaft on the flood plain of Nantahala River. Number 38 indicates 
the extensive workings on the face of Talc Mountain. Original operations at Locations 36, 37, and 38 
were separately carried on by the Nantahala Talc and Marble Company and the North Carolina Talc and 
Mining Company. The dividing line between holdings is not known, but at any rate, all operations were soon 
brought together as a single property. Operational records of the property have long since been lost, but it 
is certain that many thousands of tons of talc have been produced from the combined properties, mostly from 
the openings on the foreslope of Talc Mountain. Very few of the openings are now accessible. Attempts were 
made to reconstruct a map of the operations by consulting the many surviving people who were more or less 
intimate with the work, but descriptions were so conflicting as to be valueless. If mining is revived at any 
of the locations, it would be wise to ignore completely any information about the older openings and work 
out all problems anew. 

On Talc Mountain successive lenses of fine talc were found and mined, and the zone became a legend in 
the history of talc production because of the wealth produced. The old workings can be traced down Talc 
Mountain for nearly 1,000 feet, but can be entered at few places because of caving. A gravity tram was con- 
structed along the face of the mountain. At intervals adits were driven in to intersect the lenses and facili- 

Fig. 10. — Marble Quarry of the Nantahala Talc And Limestone Com- 
pany at Hewitt. Looking Northwest. 

Talc Deposits of the Murphy Marble Belt 51 

tate removal of the great blocks of talc. The front of Talc Mountain has a slope of about 38°, and the average 
dip of the talc was about 54°, with a plunge of 15°-30° in a southwesterly direction. Thin seams of talc led 
from lense to lense and there was no drainage problem for the operator. The lower edges of the lower lenses 
seemed to pinch out about 50 feet above the river, and a fortune was spent searching for a continuation. 
Finally, talc was discovered in a well at about 10 feet below the level of Nantahala River. A shaft (Location 
No. 37) was sunk to intercept the lense, ultimately going down to about 80 feet below the river. Here again 
was disclosed lense after lense of fine talc, though withsuch a decided plunge to the southwest that the lowest 
drifts were more than 100 feet below the river. After 10 or 12 years of operation in the new mine the water 
finally proved too much in spite of 16 pumps, powered by water wheel and steam, working day and night, 
and the mine was abandoned. Modern electric pumps, combined with systematic grouting, might now be able 
to overcome the water problem, but at that time no electric power was available. 1 

There is no organized production at the present time, but from 60 to 200 pounds of talc per day come in 
from "scavenger" operations on Talc Mountain, and a few tons of talc were found in pockets in the Hewitt 
marble quarry several years ago. Several core holes were drilled in front of the Hewitt quarry in 1946 to ex- 
plore for additional talc, but the data furnished by the cores were of little value. 


It is reported that some talc was found in Blowing Spring when U. S. Highway 19 was being rebuilt in 
1938, but these reports were not verified. 

LOCATIONS NO. 40 & 41 

These diggings were made in search of talc by Mr. Jim Bailey, of the Silvermine Community, but only 
fragments of talc-like sericite could be seen by the writer. 



A general approach to the selection of locations for talc prospecting would be to eliminate those areas 
where talc could not reasonably be expected, and then to choose from the remaining areas those localities 
which offer the best probability of success. It must be reasonably certain that the Murphy marble underlies 
those sites which are being considered. In this respect, comparison should be made with the geologic maps 
accompanying this report, and a final check should be made in the field. 

Specific locations for prospecting cannot be recommended here, other than in the form of data already 
presented, but it would be well to review some of the relationships which will control the choice of any spe- 
cific locality. 

The prospector must realize that only in comparatively flat topography does the marble lie along a 
straight outcrop or "strike line." For example, on Sheet 4 of the geologic map it will be seen that the marble 
has an extraordinarily sinuous outcrop in the rugged topography near the Nantahala River. Such irregu- 
larities are caused more by differences in the altitude of the ground surface than by differences in strike and 
dip. The reason for these irregularities can be visualized if one inclines a sheet of cardboard at 45 degrees 
(to represent a dipping bed) and proceeds to scissor strips from the two upper corners (to represent changes 
in elevation, as in two draws on either side of a ridge) ; it will be found that the trimmed edges migrate hori- 
zontally in the direction of dip. Topographic effects cannot be overemphasized, as one of the largest known 
talc bodies of the area was missed by two separate drilling programs because a "strike line" was followed 
without considering variations of surface elevation. 

The more cautious prospectors probably will avoid those places where the marble outcrop is exception- 
ally narrow, or those areas where the marble outcrop is unusually wide because of repetition by folding, unless 
there is available such definite information as exposures of talc or silicified marble, or stratigraphic data 
supplied by water wells, excavations, or previous core drilling. 

1 From a summary prepared by Mr. E. L. Miller, Jr. 


Talc Deposits of the Murphy Marble Belt 

Ordinarily, choice should not be made of sites in or near rivers, large creeks, swamps, or other places 
where water hazards are great at the start. It is well also to consider any interference that might result 
from the positions of railroads, highways, or other public and private developments. The finding of talc is of 
no consequence if the talc cannot be removed economically. 


Residual or transported deposits of clay-stained talc might best be prospected by means of pits, trenches, 
and auger holes, but these types of deposits probably would be exploited and beneficiated only in conjunction 
with an established primary talc operation. At the present time, clay-stained talc is not "commercial" in the 
Murphy marble belt. 

The most reliable and economical way to prospect for primary talc, as for similar types of concealed min- 
eral deposits, is by diamond core drilling. It is essential that drilling operations be in the hands of a com- 
petent, reputable drilling organization or crew, for it is not merely the drilling of a hole which tells the story, 
but it is the recovery and interpretation of complete and accurate information furnished by the material 
which comes from the hole, and by the action of the drill while recovering that material. With modern 
equipment, methods, and skill, a 10 per cent core loss (discounting open cavities) is excessive and unsatis- 
factory in the Murphy marble. The modern core drill is a sensitive precision tool which requires skillful 
operation and control. 

When the prospect site has been chosen, and the drilling equipment and crew assembled, an initial hole 
location must be determined. In general, this step is not so difficult as it may first appear; although work is 
directed toward the finding of a restricted talc body, the preliminary target is a zone of white, possibly talc- 
bearing marble which may be as much as 40 feet thick. This white zone is identified by the sequence of blue, 
gray, and mottled marble which is associated with it. 

Ground Surface 

y7KW%S7%fmF&777K WR&KSfflXmffl. 

Core Drill Hole 

Top of Rock 

Fig. 11. — Diagrammatic Section Showing Ideal Location of Explora- 
tory Drill Hole. 

Figure 11 is a diagrammatic cross section of the marble showing the ideal location of an initial explora- 
tion hole. The stratigraphic base (southeast contact in the usual overturned position) of the marble is at the 
right. The drill hole is located approximately one-third the distance across the marble (northwest) in order 
to obtain a good stratigraphic section of the blue, gray, mottled, and white marble sequence below top of bed 
rock. Once the position of the central white marble zone has been established, additional hole locations will 
depend upon previous results, and some drilling footage may be conserved by including less of the barren 
section in subsequent holes. It is essential, however, that the white marble zone be encountered below top of 
bed rock in order that complete core recovery may be obtained in the critical horizon. Although talc de- 
posits conceivably can continue with increased depth inside the white zone, there is an economic limit to 
depths of preliminary exploration holes, and offsets across the strike to intercept the white marble zone at 
great depths will be limited accordingly. 

Talc Deposits of the Murphy Marble Belt 


In the event that talc is intercepted, particular attention must be given to the manner in which axes of 
plunging talc bodies vary from the strike of the enclosing marble beds. For example, assume that the marble 
strikes N45°E and dips 45°SE. If the fold axes plunge 45° from the horizontal, the talc bodies will plunge 45° 
also, in a direction straight down the dip to the southeast; if the plunge is 30°, the talc bodies will plunge 30" 
in a direction more nearly south ; if the fold axes have no plunge, the talc bodies also will have no plunge and 
will be aligned exactly parallel to the strike of the marble. Comparable conditions would exist if the plunge 
were in a northeasterly direction. 

Figure 12 is a diagrammatic plan taken at some elevation below top of rock. The blue, gray, mottled, 
white, and mixed marble zones strike N45°E and dip 45°SE. Various talc bodies, which plunge 22° southeast, 
are projected up or down to the horizontal plane at which the view is taken. All of the talc bodies are contain- 
ed within the white zone which dips beneath the mottled, gray, and blue zones. Under these particular con- 
ditions, the talc bodies are aligned at an angle of about 25° with the strike of the marble. As core drilling 
progresses along the strike, holes No. 1 and No. 2 are barren, but hole No. 3 encounters talc ; a knowledge of 
the local geology indicates that the line of drilling should be changed to confirm with the probable axis of the 

^ y 25'* 

Mixed Zone 



/ Talc J© ~° ** / 

vo 4D 
QnO 2 QnO 1 

White Zone 


./; ^-" 

£-~ -^Talc 

Mottled Zone 


■y " 

/^ -* 

Gray Zone 

*— "*-Talc 

(Strike = N45'E) 

Blue Zone 

Fig. 12. — Diagrammatic Plan Detail of Orientation of Talc Bodies 
and Drilling Control. Plan is Taken at An Elevation Be- 
low Top of Rock. Note. Talc Bodies Are Contained Entire- 
ly Within the White Zone and Plunge Beneath the Mot- 
tled, Gray, and Blue Zones. 

talc body, and hole No. 4a is drilled down the plunge. If this hole had been barren, the next choice would have 
been a location in the opposite direction, up the plunge. Finally, once talc is discovered, the body should be 
completely delimited before any thought is given to the sinking of a shaft. 

The foregoing discussions are intended to be explanatory rather than categorical. Exploration for con- 
cealed deposits does not comprise the mechanical application of "cookbook" rules and methods ; to the con- 
trary, a maximum of technical knowledge, resourcefulness, and intuition is required if any measure of suc- 
cess is to be achieved. As regards technical knowledge, if the data submitted here are to be used to any ad- 
vantage, it is essential that geological control be exercised in all phases of talc exploration. Drill holes must 
be located to best advantage and cores must be adequately logged and interpreted for maximum utilization of 
"dry" holes. Geologic sections and subsurface plans should be prepared. In addition, the competent geologist, 
by means of intuition developed through experience, often can predict a little beyond tangible data. Much 
of these types of assistance is available from various public agencies and full advantage should be taken of 
them. In the event that some time must elapse between the gathering of information and the examination of 
the data by competent authorities, it is especially needful that all data and material be kept in as perfect con- 
dition as possible. It never hurts even to carry the most minute precautions almost to an extreme. 

One final word applies to all forms of mining ventures. It is never wise to risk more than one can afford 
to lose. 

54 Talc Deposits of the Murphy Marble Belt 


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